۲ — —-—-— Pot وین‎ NT tari e وود‎ Dee erc VOLUME 91, NUMBER 6 NOVEMBER 10, 1986 from North American Geologic Terranes 82 E. A. Pessagno, Jr., P. A. Whalen, and K.-Y. Yeh Jurassic Nassellariina (Radiolaria) by Paleontological Research Institution 1259 Trumansburg Road Ithaca, New York, 14850 U.S.A. PALEONTOLOGICAL RESEARCH INSTITUTION Officers RESIDENT EEN WILLIAM P. S. VENTRESS e Bg a ue tI CO TE JAMES E. SORAUF SJ HENRY W. THEISEN i e A ne ES JAMES C. SHOWACRE r DAE o MC a GE UIS: JOHN L. CISNE RECIO d PETER R. HOOVER EE وا‎ TT HENRY W. THEISEN Trustees BRUCE M. BELL (to 6/30/87) CATHRYN NEWTON (to 6/30/88) RICHARD E. BYRD (to 6/30/89) WILLIAM A. OLIVER, JR. (to 6/30/89) JOHN L. CISNE (to 6/30/88) EDWARD B. Picou, JR. (to 6/30/89) J. THOMAS DUTRO, JR. (to 6/30/87) JAMES E. SORAUF (to 6/30/88) Harry A. LEFFINGWELL (to 6/30/87) HENRY W. THEISEN (to 6/30/89) ROBERT M. LINSLEY (to 6/30/89) RAYMOND VAN HOUTTE (to 6/30/88) A. MCCUNE (to 6/30/87) WILLIAM P. S. VENTRESS (to 6/30/87) A. D. 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Hoover Director Paleontological Research Institution 1259 Trumansburg Road Ithaca, New York 14850 U.S.A. 607-273-6623 VOLUME 91, NUMBER 326 NOVEMBER 10, 1986 from North American Geologic Terranes E. A. Pessagno, Jr., P. A. Whalen, and K.-Y. Yeh Jurassic Nassellariina (Radiolaria) by Paleontological Research Institution CORB BUD TO 1259 Trumansburg Road ES 1.G.C.P. #171 UNES[HO Ithaca, New York, 14850 U.S.A. Circum-Pacific Jurassic Library of Congress Card Number: 86-62817 Printed in the United States of America Allen Press, Inc. Lawrence, KS 66044 U.S.A. CONTENTS Page d 5 ee en een SE 9 he e a 소재 ON 6 Tectonostratigraphy and the Faunal Mosaic of the Western Cor- SUIS LAN NC RTO Mig S EE ji Wrangellia Terrane, Queen Charlotte Islands, British Colum- P1111 d ER eie 10 Stratigraphic Summary KET eee, 13 a mer ee ee 18 Blue Mountains Province of Northeast and East-central EI DE 108) Stratigraphic Summary, Suplee-Izee Area ............. 14 ات لا‎ BOLU ata tc ace uU UE T 14 ERY GOP koh Wah GUO Mer tenes ceria cx esc monte E ae 14 ß TS 15 , I eh 15 , UU UE 15 SOUTO Mice E treet ee ER 15 LONESOME OCU e en UI A 16 The Coast Range Ophiolite and Associated Strata, California Coast Ranges Fw! 16 ae ʒ eet ERO ADS 19 Stratigraphic Summary Dann OS O 19 Vizcaino Peninsula, Baja California Sur, Mexico ......... 20 Stratigraphic Summary San TIDONG Bormaton ⁰ʒ UR RS S 20 ga o O ee 20 TANG SUOG Member en 20 E o e EO RE DEE 20 Sandstone: MEMO o y RS os 20 Systematic Paleontology ¡MANCHES AE 21 PEST CONST نت‎ ee E EA AA AA E AE AEN E 21 Suborder Nassellariina FSI با‎ PALA. e as 22 (ens SEC CUS UCN ee ee aS GETS e eee Me CONG nn ess at 26 Family Hilarisiregidae Takemura and Nakaseko ........ 29 Genus Hilarisirex Takemura and Nakaseko .......... 30 BamnıyzUltranapondaePessaeno nn... 32 موی‎ IC NOE CG a aA 32 ee e ER 34 Appendix — Locality fs. ee wen 46 EMEA A 52 EE 37 Ende ی‎ y 68 Text-figure LIST OF ILLUSTRATIONS Page 1. Map showing distribution of geologic terranes in the Blue Mountains Province .......... 6... e sent nn 7 2. Models showing the relationship of radiolarian diversity and abundance to their paleolatitudinal distributions in the Middle and Late 가비 OR 7 ß ß un tue Seren an foe rats 8 ~ ndieators , POTC 2. na ß 10 4. Maps showing some of the localities described in this reporrtᷣꝝ i.... 12 5. Occurrence of Lower Jurassic Nassellariina in east-central Oregon, California, the Queen Charlotte Islands, and NG a EE ee tc aang ta tet Rah CAS 24 6. Occurrence of Middle and Upper Jurassic Nassellariina in east-central Oregon, California, and east-central Mexico ............... 27 7 . Range zones of Lower, Middle, and Upper Jurassic species assignable to the Farcidae, Ultranaporidae, and Hilarisiregidae JJ و و‎ IN les ES ET NATA en O O O ĩ E E E. foldout inside back cover JURASSIC NASSELLARIINA (RADIOLARIA) FROM NORTH AMERICAN GEOLOGIC TERRANES! By E. A. PESSAGNO, JR.,? PATRICIA A. WHALEN,” AND KUEI-YU YEH? ABSTRACT Much of the western part of the Cordilleran Region of North America is characterized by geologic terranes which originated at low latitudes and were displaced to higher latitudes during the Late Paleozoic and Mesozoic. Many of these terranes such as the Wrangellia terrane have been displaced hundreds or even thousands of kilometers from lower, near-equatorial latitudes to their present positions. The magnitude of the tectonic complexity of the western Cordilleran Region is immense. Obviously, paleontologists must consider the displaced terrane problem in their attempts to compile meaningful biostratigraphic zonations and zoogeographic reconstructions for the Mesozoic of this region and indeed, the entire Circum-Pacific margin. The potential utility of Radiolaria in Mesozoic biostratigraphic and paleo-oceanographic studies and in geology in general is enormous. Radiolarian zonal schemes now rival those of the ammonites in parts of the Jurassic and Cretaceous. Furthermore, even though the study of Jurassic Radiolaria is still in its infancy, it is now apparent that at least for the Middle and Upper Jurassic, Radiolaria can be utilized to differentiate the Tethyan Realm from the Boreal Realm and to subdivide each of these faunal realms into provinces. On the basis of simple criteria we subdivide the Tethyan Realm into: (1) A Central Tethyan Province characterized by the presence of Ristola Pessagno and Whalen, 1982, the absence of Parvicingula Pessagno, 1977a, and high pantanelliid diversity; and (2) a Northern Tethyan Province, characterized by common Parvicingula and high pantanelliid diversity. The radiolarian assemblage of the Boreal Realm during the Middle and Late Jurassic is characterized by the presence of abundant Parvicingula and by low pantanelliid diversity. The Boreal Realm is in turn subdivided into a Southern Boreal Province where pantanelliids still persist and a Northern Boreal Province where pantanelliids appear to be absent. Using these simple criteria together with megafossil and paleomagnetic data (where available), we have been able to chart the course of various displaced terranes from low to higher latitudes during the course of Jurassic time. In the terranes of the Blue Mountains Province of eastern Oregon, both the radiolarian and ammonite assemblages reflect a change from Tethyan (Northern Tethyan Province) to Boreal (Southern Boreal Province) during the late Bathonian/Callovian. The first or final appearances of many taxa occurring in the late Bajocian — Bathonian — Callovian may, in fact, be paleolatitudinally controlled and may not reflect their total range in Boreal or Tethyan strata. Most of the taxa included in the Systematic Paleontology herein are described from geologic terranes that have been displaced from low (Tethyan) latitudes to higher (Boreal) latitudes during Jurassic times. Two new genera (Farcus, n. gen., and Rolumbus, n. gen.) and thirty-four new species (Farcus asperoensis, n. sp., F. graylockensis, n. sp., Rolumbus gastili, n. sp., R. hamiltoni, n. Sp., R. halseyensis, n: sp., R. mirus, n. sp., R. venustus, n. Sp., Hilarisirex inflatus, n. sp., H. oregonensis, n. sp., Jacus reiferensis, n. sp., J.(?) sandspitensis, n. sp., Napora antelopensis, n. sp., N. baumgartneri, n. sp., N. bearensis, n. sp., N. bona, n. sp., N. boneti, n. sp., N. browni, n. sp., N. burckhardti, n. sp., N. cerromesaensis, n. sp., N. cosmica, n. sp., N. fructuosa, n. sp., N. (?) graybayensis, n. sp., N. heimi, n. sp., N. horrida, n. sp., N. insolita, n. sp., N. izeensis, n. sp., N. maritima, n. sp., N. mitrata, n. sp., N. moctezumaensis, n. sp., N. morganensis, n. sp., N. opaca, n. Sp., N. tumultuosa, n. sp., N. turgida, n. sp., and N. vegaensis, n. sp.) have been described among the nassellarian families Farcidae, n. fam., Hilarisiregidae Takemura and Nakaseko, 1982, and Ultranaporidae Pessagno, 1977b. In an effort to formulate a more phylogenetic classification for these families and their included genera, we have stressed test construction as the primary basis for their definition. Many of the species and genera figured in this report are distinctive and short ranging; as a result, they should prove useful in compiling a detailed radiolarian zonation for the Jurassic. Range zone data are presented for all taxa. Where known, the distribution of taxa within the Tethyan and Boreal realms is indicated in the text and text-figures. ACKNOWLEDGMENTS duction Research Company and the Mobil Oil Cor- poration. The authors wish to thank the following persons for their help during the course of this project: Dr. C. A. Hopson (Univ. of California, Santa Barbara, CA) for his helpful discussions and for his aid in collecting samples from radiolarian-bearing strata associated with This project has been supported by grants from the National Science Foundation (GA-35094, DES-72- 01528-A01, EAR-76-22029, EAR-77-22457, EAR-78- 12934, EAR-8121550, EAR-8305894) and by funding from the Atlantic Richfield Company, the Exxon Pro- ! Contribution Number 464, Program for Geosciences, The Uni- the Coast Range ophiolite; Dr. D. L. Jones (Univ. of versity of Texas at Dallas. California, Berkeley, CA) for pointing us toward Wran- ? Program for Geosciences, The University of Texas at Dallas, gellia; Dr. W. R. Dickinson (Dept. o € Geosciences Richardson, TX 75080. 3 National Museum of Natural Science, 1 Kuan Ch’ien Rd., Tai- chung, Taiwan, R. O. C. Univ. Arizona, Tucson, AZ) for advice pertaining to the geology of the Suplee-Izee area, east-central Ore- gon; Dr. R. Imlay (U. S. Geol. Survey, Washington, DC) for his advice pertaining to the geology and Ju- rassic stratigraphy of east-central Oregon and for his identification of ammonites; Dr. P. Smith (Dept. Ge- ology, Univ. of British Columbia, Vancouver, BC, Canada) for his identification of ammonites and for supplying us with useful biostratigraphic data from the Suplee-Izee area; Mr. N. MacLeod (Univ. of Texas at Dallas, Richardson, TX) for his advice pertaining to the stratigraphy ofthe Snowshoe Formation (east-cen- tral Oregon); Mr. W. T. Rothwell (formerly Univ. of Texas at Dallas, Richardson, TX) for his care in pro- ducing many ofthe scanning electron micrographs; Mr. W.M. Six (Univ. of Texas at Dallas, Richardson, TX) for his care in producing many ofthe scanning electron micrographs and preparing the text-figures; Dr. H. W. Tipper (Geol. Survey of Canada, Vancouver, BC, Can- ada), Mr. B. E. B. Cameron (Geol. Survey of Canada, Sidney, BC, Canada) and Ms. E. S. Carter (Dept. Ge- ology, Univ. of British Columbia, Vancouver, BC, Canada) for their advice pertaining to the stratigraphy ofthe Maude Formation, Queen Charlotte Islands, BC, Canada. Dr. Tipper is also thanked for his identifica- tion and dating of ammonites from the Kunga and Maude formations; Dr. J. F. Longoria (Univ. of Texas at Dallas, Richardson, TX) for his advice pertaining to the Upper Cretaceous stratigraphy of the Vizcaino Peninsula (Baja California Sur); and Dr. Y. Cheng (Na- tional Museum of Natural Science, Taichung, Taiwan, R. O. C.) for printing the photographs for the plates. Finally, we wish to express our appreciation to Dr. C. D. Blome (U. S. Geol. Survey, Denver, CO) and Dr. G. E. G. Westermann (McMaster University, Hamilton, ON, Canada) for reviewing the manuscript. INTRODUCTION The study of Jurassic Radiolaria is still in its infancy. Except for a few reports at the turn of the century by workers such as Rüst (1885, 1898), Parona (1890), and Vinassa de Regny (1899), no other comprehensive studies dealing with Jurassic Radiolaria were published until the 1970's (e. g., Foreman, 1973; Pessagno, 1977a). Investigations completed (Pessagno and Blome, 1980; Baumgartner, 1980a; Baumgartner, De Wever, and Kocher, 1980; Pessagno and Poisson, 1981; Pessagno and Whalen, 1982; Pessagno and Blome, 1982; De Wever, 1982; Baumgartner, 1984; Blome, 1984b) and in progress indicate that the Jurassic assemblage from both the Tethyan Realm and the southern part of the Boreal Realm is quite diversified. It is not uncommon to find as many as 60 to 150 species-level taxa in well- preserved assemblages. In spite of the recent surge of investigations, approximately 85 percent of the total Jurassic assemblage remains undescribed. BULLETIN 326 The potential of these planktonic microfossils for Mesozoic stratigraphy and for geology in general is immense. Radiolarian zonal schemes now being com- piled by Baumgartner (1984) and Pessagno, Blome, Carter, MacLeod, Whalen, and Yeh [in press] rival those of the ammonite workers in many parts of the Jurassic succession. For example, in the Middle Ju- rassic succession of east-central Oregon (Suplee—Izee Area, John Day Inlier) Smith (1980, p. 1606, fig. 4) included Bajocian strata in five ammonite zones; Pes- sagno, Blome, Carter, MacLeod, Whalen, and Yeh [in press] divide the Bajocian into four radiolarian zones. As more stratigraphically-useful taxa are described, it is likely that the resolution of the radiolarian zonation for the Bajocian will be even further enhanced. In compiling a zonal scheme for the Jurassic we are attempting to calibrate our radiolarian biostratigraphy with that of the ammonites and other well-studied fos- sil groups (e.g., the calpionellids; see Pessagno, Blome, and Longoria, 1984). We are defining radiolarian zonal units using taxa with tests sufficiently sturdy to be pre- served not only in residues extracted from limestones, but also in residues extracted from cherts and shales. Furthermore, where possible, we define zonal units utilizing taxa that bridge the Boreal and Tethyan realms. A zonal scheme so contrived should prove invaluable in interpreting the stratigraphy and ultimately the com- plex structure of radiolarian-chert-bearing terranes in western North America. In addition to their use in biostratigraphic studies it is now obvious that Jurassic Radiolaria can be useful in delimiting faunal realms, or in some cases, provinces within realms. For example, for the Middle and Late Jurassic, it is possible to differentiate a Central Tethyan Province from a Northern Tethyan Province and to delimit the boundary between the Tethyan and Boreal realms. In spite of the fact that the study of Jurassic Radiolaria and indeed all Mesozoic Radiolaria is still in its infancy, it is apparent that this group of micro- fossils offers great potential in paleolatitudinal studies. It is also apparent that the radiolarian faunal data, together with those of other fossil groups, should be useful in helping tectonocists recognize displaced ter- ranes and in charting the courses of such terranes throughout the course of the Mesozoic (see Tectono- stratigraphy). The present report focuses on three important family groups: the Farcidae, n. fam., the Hilarisiregidae Ta- kemura and Nakaseko, 1982, and the Ultranaporidae Pessagno, 1977b. The first two families are restricted to the Jurassic whereas the range of the third family extends into the Cretaceous. Many species-level taxa of all three families are short-ranging and distinctive and should be useful in formulating a zonation for the JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 7 North American Jurassic. Samples that we have stud- ied for the purpose of this project come from east- central Oregon (Suplee-Izee Area, John Day Inlier), the Queen Charlotte Islands, east-central Mexico, and Baja California Sur. TECTONOSTRATIGRAPHY AND THE FAUNAL MOSAIC OF THE WESTERN CORDILLERAN REGION The western part of the Cordilleran Region is a col- lage of displaced terranes that have been accreted to the craton during the Paleozoic and Mesozoic. Many large terranes (e.g., Wrangellia) have been displaced hundreds or even thousands of kilometers from their point of origin (Jones, Silberling, and Hillhouse, 1977). Pessagno and Blome (1986) suggested that the driving mechanisms for such large scale displacements are megashears such as those that crosscut Mexico in a northwest-southeast direction (Longoria, 1984, 1985). Moreover, they suggested that many of the larger ter- ranes such as Wrangellia, the Blue Mountains terrane, and the Sierran terranes originated at low latitudes and gradually moved northward along megashear systems during the course of the Mesozoic. The faunal record of the aforementioned terranes is remarkably similar. It is noteworthy that all of these terranes display dom- I A Snoke E River 4 WASHINGTON | Mr v ING [2 WALLOWA MOUNTAINS LIN OREGON \ per RER AN O Kilometers 100 L— —À— — —ÁH— SOT CMT MCT HAT < ZA Ea Ei SSSSS SEVEN CENTRAL MESOZOIC HUNTINGTON DEVILS MELANGE CLASTIC ARC TERRANE TERRANE TERRANE TERRANE Text-figure 1.—Map showing distribution of geologic terranes in the Blue Mountains Province of east-central and northeastern Or- egon, southeastern Washington, and northwestern Idaho (modified from Dickinson, 1979). inantly Tethyan faunas at least until the end of the Bajocian. By the late Bathonian or Callovian, Boreal faunas predominate. As indicated by Pessagno and Blome (1986), the shift of these terranes to higher lat- itudes is coincident with the opening of the Gulf of Mexico during the late Bathonian or Callovian. Triassic, Jurassic, and Lower Cretaceous red, man- ganiferous ribbon cherts, which occur in ophiolites and in subduction complexes from Baja California to Alas- ka, all contain Tethyan (dominantly Central Tethyan; see below) radiolarian assemblages (Pessagno, Blome, and Longoria, 1984, p. 20). In the melange of the Fran- ciscan Complex (California Coast Ranges) or the Pa- cific Rim Complex (Vancouver Island), it is not un- common to find masses of red ribbon chert containing Central Tethyan Radiolaria adjacent to blocks of flyschoid sandstone and shale containing Buchia Rouillier, 1845, and Boreal Radiolaria. The spectrum of complexity resulting from latitudinally-displaced terranes in the western part of the Cordilleran Region is thus immense. Obviously, it makes biostratigraphic analysis difficult and broad-scale zoogeographic recon- structions impossible. Before the introduction of the displaced-terrane hy- pothesis by Jones, Silberling, and Hillhouse (1977), most attempts to discuss the Jurassic faunas of the Circum-Pacific Region were at best chaotic and ended in bizarre zoogeographic reconstructions. Hölder (1979, p. A391), for example, in discussing Jurassic marine zoogeography, described the Circum-Pacific Jurassic as lacking faunistic uniformity; in fact, he (p. A401) went as far as entitling a section of his chapter: “Faunal Mosaic of the Pacific Ocean”. Recognition of displaced terranes depends primarily on paleolatitudinal data derived either from paleo- magnetism or paleontology. Taylor et al. (1984, p. 122) noted that “Faunal analysis can thus, in favourable cases, provide the following indications that are often beyond the reach of paleomagnetic studies. It can (a) decide whether a terrane at a given time was in the northern or southern hemisphere, thereby placing con- straints on the polarity of paleomagnetic determina- tions; (b) indicate displacements of as little as a few hundred kilometers; and (c) provide longitudinal con- straints." The longitudinal constraints offered by fau- nal analysis are definitely beyond the reach of paleo- magnetism and should be heeded by all geologists attempting to determine the origin of a displaced ter- rane. For example, the Tethyan bivalve Weyla Boehm, 1922, occurs in Lower Jurassic strata from Chile to Alaska (Damborenea and Mancenido, 1979; Pessagno and Blome, 1986); it does not occur in the western Pacific. Weyla occurs in the Lower Jurassic of the Sier- ran terranes, the Mesozoic clastic terrane (Blue Moun- 8 BULLETIN 326 tains Province), and Wrangellia (Imlay, 1968, 1980; Pessagno and Blome, 1986; Taylor et al., 1984). This, as well as other faunal evidence, indicates that these terranes originated in the eastern Pacific. Pessagno, Blome, and Longoria (1984, pp. 19-20) and Pessagno and Blome (1986) developed simple cri- teria for differentiating the radiolarian assemblage of the Tethyan Realm from that of the Boreal Realm (Text-figs. 2, 3). Furthermore, they subdivided each of these faunal realms into provinces. The Tethyan Realm was subdivided into (1) a Central Tethyan Province characterized by the presence of Ristola Pessagno and Whalen, 1982, and high pantanelliid abundance and diversity and (2) a Northern Tethyan Province char- acterized by the presence of common Parvicingula Pes- sagno, 1977a (sensu Pessagno and Whalen, 1982) and high pantanelliid abundance and diversity. They sub- divided the Boreal Realm into (1) a Southern Boreal Province delimited by abundant and diversified Par- vicingula and a dramatic drop in pantanelliid abun- dance and diversity and (2) a Northern Boreal Province distinguished by abundant Parvicingula and by a total lack of pantanelliids. In general, pantanelliid diversity is three or four times greater in the Tethyan Realm than it is in the Southern Boreal Province. This esti- mate is based on analyses of well-preserved material extracted from limestone samples from east-central Mexico (Northern Tethyan), Greece (Central Tethyan), the California Coast Ranges (Southern Boreal), and the Klamath Mountains (California; Southern Boreal). Many, but not all, radiolarian chert samples are too diagenetically altered to allow the recovery of well- preserved pantanelliids and other fragile Radiolaria; usually only Radiolaria with very sturdy tests (e.g., Mirifusus Pessagno, 1977a) are preserved. Because of the displaced terrane problem, Pessagno and Blome (1986) treated all megafossil data from the western part of the Cordilleran Region as suspect un- less faunal associations or paleomagnetic data were cited. Moreover, in their discussions of the Triassic and Jurassic faunas of the Blue Mountains Province (eastern Oregon and western Idaho), they evaluated the megafossil data in light of the distribution of taxa in areas that have not been greatly displaced latitudi- nally (e.g., the western interior of North America; west- ern Europe). In addition, they utilized the paleo-ocean- ographic reconstructions of Gordon (1974) and the paleolatitudinal maps of Smith, Hurley, and Briden (1981) in their interpretations. One must, however, keep in mind that cratonic North America was situated at lower latitudes during the Triassic and Early Jurassic than it was during Middle and Late Jurassic times. With the movement of the craton in a northerly di- rection during the Triassic and Jurassic, paleolatitu- dinal lines, faunal realm, and faunal province bound- aries shifted progressively to the south (see Smith, Hurley, and Briden, 1981). The boundary between the Tethyan and Boreal Realms was situated at approximately 30°N during the Jurassic (Pessagno, Longoria, MacLeod, and Six, [in Text-figure 2.—Models showing the relationship of radiolarian diversity and abundance to their paleolatitudinal distributions in the Middle and Late Jurassic of western North America. A — Model depicting pantanelliid diversity during the Middle and Late Jurassic. Well-preserved Tethyan pantanelliid assemblages pos- sess three or four times more species-level taxa (described and un- described forms) that those in the Southern Boreal Province (Boreal Realm). Our data indicate that pantanelliids are absent in the North- ern Boreal Province. B—Model showing distribution of Parvicingula Pessagno, 1977a (sensu Pessagno and Whalen, 1982) and Ristola Pessagno and Wha- len, 1982, during Middle and Late Jurassic times. Central Tethyan Province faunas lack Parvicingula and are characterized by the pres- ence of Ristola. Northern Tethyan and Boreal Province faunas con- tain both Parvicingula and Ristola. Parvicingula is the dominant element among the Parvicingulidae Pessagno, 1977a (sensu Pessagno and Whalen, 1982) in the Boreal Realm. 0 = Data from North Slope/Brooks Range and Puale Bay areas of Alaska. At Puale Bay, Blome (1984b) has recovered well-preserved middle Callovian Radiolaria occurring at the same horizon as Sten- ocadoceras Imlay, 1953. Stenocadoceras is a high-latitude Boreal ammonite taxon that occurs elsewhere in Russia and Greenland; 1 = Data from the upper half of volcanogenic-pelagic successions over- lying the Coast Range ophiolite, from the Great Valley Supergroup (California Coast Ranges), from the Galice Formation s. /. (Klamath Mountains, California), and from the Upper Jurassic (upper Ti- thonian) part of the Eugenia Formation, Vizcaino Peninsula, Baja California Sur, Mexico. Common to abundant Buchia Rouillier, 1845, are associated with the radiolarian faunas in the Great Valley Supergroup, the Galice Formation, and the Eugenia Formation; 2 = Data from the Taman and Pimienta formations of east-central Mex- ico. Radiolarian faunas here are associated with Tethyan ammonites, pectenacids (e.g., Aulacomyella Furlani, 1910), calpionellids, and nannoconids. Upper Jurassic Mexican radiolarian faunas from this area are characterized by high pantanelliid diversity and the presence of common Parvicingula Pessagno, 1977a. Other data from Lower Jurassic (Toarcian) and Middle Jurassic (Aalenian to upper Bajocian) portion of Snowshoe Formation (Blue Mountains Province, east- central Oregon; p. 14 herein); 3 = Data from the Mediterranean area, Turkey, Iran, Oman, Tibet, and various Deep-Sea Drilling Project sites in the North Atlantic (e.g., Site 367, Cape Verde Basin; Site 534, Blake-Bahama Basin; Baumgartner, 1984). Central Tethyan Province radiolarian faunas lack Parvicingula Pessagno, 1977a (sen- su Pessagno and Whalen, 1982) and also, when well-preserved, dis- play high pantanelliid diversity. No Central Tethyan Province faunas are known from North America except from displaced terranes and subduction complexes (e.g, Coast Range ophiolite and overlying volcanogenic-pelagic strata, Franciscan Complex, California; Pacific Rim complex, Vancouver Island, British Columbia); 4 — No data from the southern hemisphere. Model assumes symmetrical arrange- ment of faunal provinces and realms north and south of Middle to Upper Jurassic paleoequator. Boundary between Central and North- ern Tethyan Provinces is placed at approximately 22 degrees North. Boundary between Tethyan and Boreal Realms is placed at approx- imately 30 degrees North. Obviously, fluctuations of all of these boundaries are likely to occur relative to a given paleolatitudinal position due to differences in oceanic circulation. Ju R A SS IC N A SS EL LA R IIN. Al Pines A G N 0 , W H A LE N „A N D Y E H pre Sai ample, In pi ا‎ th an 10 [S d ne $ L G we ate ran s) ur J d a re ur yaris en P ی‎ Te late nd atin Tith ; n stri th 01 $m bu e OSSi or tio Sc sils ex n coti (i 7 in as .6 w h Ü est elf ern E u Ja rope 3 te ri D R nd T de e t eth n, ma os e ne upp P D. and ort d en ce ound d TL ——— al en í T th Woh 19 eth € ey 7i yan No „an 5 Pr. rth d a mg in ce Ó < a 00 208 z 855989 5 9995 o m p < SS o 08880 888888 0 a nn 8888 ° 888 2 b ° 250896 s s 23980: < ee 888 808 o 888889 8889 $9 808 8888 808 p ec 00 28080 o dm COD Get 00 a 8889 oO 88888 S o9. 808 SOS 9885855 888 sieh] 09 0 nn 8888 $85 BO 69 faa 895888 28080 828289 9888878 888 o m 98885 - 0 390 P > 988299 SE 886 2020 0° A = 98885 09 $08 3 dm N a a oos 898 888 gas o 805 588 00 o 6 888 T z s 888 0280823 8888 o9 = 09000 698 09 | 8888 09 T 9888858 888885 oe 888 o9 E. o 8828863 o9. 888 888 888 1 o 888 | o < o nn 6 ui | 28888 888 gas 828988 T | ae dus d SE 09 ~- oe o9 3 Bas 800 8888 z uu aa 28080 = 8858533 888 a 9595 00000 ee 00 98888 808 a 9 o 828888 | 00 1 o o9 $08 888 o 6 898 O Ge 895 _ o9 oa 888 o9 O 828898 O 28080 T o 7 E CE 885899 | T TH N EI Sog 892 Y T 2020 898 888 o9 A RA 8888 9985858 N L 888885 898 00 208909 POP 8888 Y PR oe 8888 o 0. 888885 5 A V | d o9 IN 8888 898 8887 c N RE z 888895 3 A ۳ 608 88 N oY 50 o9 LM ETH OR 060 0° YA TH E 0 (P N ER 208 9888858 o9 A p N 202 888 8888 See a ) V o IN | CE 3 | 8585 m + B 8 5% 이 O O A980 R U 53898 EA TH 0908 B L ER 86969 = : movi = ee LM AL — puoi; IN 0 R E A SE IN D IV E EN: A N D A B UN D A NC E o N v 8 Do N 0 DER RN T E en PROV IN C E T ET H Y A N REAL M (PA RT ) > TE TH Y A N E V IN @ E BO R EA 4 PR 0 V IN 77 N 6 0 ی‎ oht PR RN O V IN e E so mm R N BO R E A L R EALM (PA RT ) 10 BULLETIN 326 is placed at approximately 22°N in eastern Mexico. Mexican strata containing Northern Tethyan radiolar- ian faunas also contain calpionellids as well as Tethyan ammonites and bivalves (Pessagno, Longoria, Mac- Leod, and Six [in press]). This estimate takes into ac- count the southeasterly displacement of Northern Tethyan strata (e.g., Taman Formation) in Puebla, Hil- dalgo, Veracruz, and San Luis Potosi along megashear systems (see Longoria, 1984, 1985). Jurassic (mostly Late Jurassic) Central Tethyan radiolarian faunas oc- cur in Oman, Iran, Turkey, and throughout the Med- iterranean area (see, e.g., Tippit, 1981; Baumgartner, 1984). Late Jurassic Central Tethyan faunas also occur in the Cape Verde Basin and the Blake-Bahama Basin in the North Atlantic (Baumgartner, De Wever, and Kocher, 1980; Baumgartner, 1984). As already noted, Middle and Late Jurassic Central Tethyan faunas occur in red ribbon cherts commonly associated with sub- duction complexes around much of the Circum-Pacific margin (Baja California to Alaska, Japan, East Indies). Central Tethyan faunas likewise occur in Late Jurassic tuffaceous cherts overlying the Coast Range ophiolite (California; Pessagno, Blome, and Longoria, 1984). No definitely autochthonous Central Tethyan faunas are known from North America. Northern Tethyan radi- olarian faunas are known from Late Jurassic strata in the California Coast Ranges, western Oregon, east-cen- tral Mexico, and northeastern Mexico (Pessagno, Blome, and Longoria, 1984; Pessagno, Longoria, MacLeod, and Six [in press]). They are also well rep- resented in the Early Jurassic (Toarcian) and Middle Jurassic (Aalenian, Bajocian) of east-central Oregon (Pessagno and Blome, 1980; Pessagno and Whalen, 1982; Pessagno and Blome, 1986). To date, Northern Tethyan faunas have not been reported from western Europe. Southern Boreal radiolarian faunas are presently only known from North American terranes. They occur in the Late Jurassic strata of the California Coast Ranges (Pessagno, 1977a; Pessagno, Blome, and Longoria, 1984), Klamath Mountains of California (Pessagno, unpublished data), and the Vizcaino Peninsula of Baja California Sur, Mexico (Davila, 1986). They are also well represented in the Middle Jurassic (Bathonian, Callovian) of east-central Oregon (terranes of the Blue Mountains Province; Pessagno and Blome, 1986). In the Late Jurassic, the Southern Boreal assemblage is usually associated with abundant Buchia Rouillier, 1845. The Northern Boreal assemblage is known from the Jurassic of the Alaskan Peninsula (Puale Bay; Blome, 1984b), southwestern Alaska (Pessagno, un- published data), and the North Slope of Alaska (Pes- sagno, unpublished data). At Puale Bay Blome’s very well-preserved Northern Boreal assemblage is associ- ated with Stenocadoceras (Imlay, 1953). Stenocado- ceras is a high latitude Boreal ammonite taxon, which is known elsewhere from Russia and Greenland (Ar- kell, Kummel, and Wright, 1957, p. L302; Taylor et al., 1984, p. 133, fig. 16). “Tethyan Realm” and “Boreal Realm” as used in this report correspond for the most part to the usage of Taylor et al. (1984). However, some differences are evident particularly in the Late Jurassic (late Oxfordian to late Tithonian). For example, the late Tithonian portion of the Great Valley Supergroup (California Coast Ranges) would be regarded by these authors as Tethyan because it contains ammonites such as Koss- matia Uhlig, 1907, Parodontoceras Spath, 1923, and Proniceras Burckhardt, 1919. We regard these strata as Southern Boreal because they lack calpionellids and contain abundant Buchia Rouillier, 1845, in associa- tion with abundant Parvicingula Pessagno, 1977a (sen- su Pessagno and Whalen, 1982) and poorly-diversified pantanelliids. In contrast, we agree closely with Taylor et al. (1984) in the differentiation of Tethyan and Bo- real strata in the John Day Inlier (Blue Mountains Province, east-central Oregon; see below). Other realms and provinces noted by these authors cannot be dis- tinguished at present through our analysis of the Ju- rassic radiolarian assemblage. Terranes from which our radiolarian faunas are de- rived in this report are discussed below. All of these terranes have been displaced to some degree paleolat- itudinally. WRANGELLIA TERRANE, QUEEN CHARLOTTE ISLANDS, BRITISH COLUMBIA The Queen Charlotte Islands (Text-fig. 4) are part of the Wrangellia terrane of Jones, Silberling, and Hill- house (1977). Paleomagnetic data presented by Jones, Silberling, and Hillhouse (1977) indicate that Wran- gellia originated 15° north or south of the Triassic pa- leoequator. During the Late Triassic and Early Jurassic both the molluscan and radiolarian assemblages tend to be predominantly Tethyan (Tipper, 1981; Taylor et al., 1984; Pessagno and Blome, 1986). However, the presence of very rare Boreal ammonites (amaltheids) in the upper Pliensbachian portion of the Maude For- mation suggests that the Queen Charlotte Islands com- ponent of Wrangellia was situated in the northern hemisphere (Taylor et al., 1984, pp. 128, 135). The radiolarian assemblage during the Late Triassic (No- rian) and Early Jurassic (Hettangian to Toarcian) is characterized by an abundant, diversified pantanelliid Text-figure 3.—Indicators of faunal realms and provinces. Dis- tribution of selected radiolarian and megafossil taxa, and various other microfossils (e.g., calpionellids) in faunal realms and provinces during the Middle and Late Jurassic. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 11 TETHYAN FAUNAL REALM BOREAL FAUNAL REALM SOUTHERN CENTRAL NORTHERN | SOUTHERN NORTHERN TETHYAN TETHYAN TETHYAN BOREAL BOREAL PROVINCE UN S PROVINCE | PROVINCE PROVINCE ? Mirifusus Pessagno, 1977a ; 7 | Parvicingula Pessagno, 1977a D ? Ristola Pessagno & Whalen, 1982 2 ; 2 E 2 2? Hsuum Pessagno, 1977a ۱ Y i H x و‎ _Perispyridium DU HEE 1978 3 j D — E Y N y H = a Turanta Pessagno & Blome, 1982 ; — 8 2? Napora Pessagno, 1977a x z E 2 7 T y 7 = A Q Hilarisirex Takemura & Nakaseko, 1982 * a 2? Pantanellium Pessagno ,1977a : E e 0 Q Trillus Pessagno & Blome, 1980 pi * N 2 83 2 ZartuS Pessagno & Blome, 1980 5 S E „ Emiluvia Foreman, 1973 1 : b y H , E ai Tripocyclia Haeckel, 1881 m و‎ Acanthocircus dicranocanthus Squinabol, 1914 N T H N al Podocapsa amphitreptera Foreman, 1973 o “Eucyrtidium” ptyctum Riedel & Sanfilippo, 1974 3 un fa Buchia Rouillier, 1845 S = و‎ Aulacomyella Furlani, 1910 > 7 m „ al Kossmatia Uhlig, 1907 D 4 E Glochiceras Hyatt, 1900 N ^ H A 3 | > __doceras Burckhardt, 1906 = Amoebites Buckman, 1925 bd z 3 Cardioceras Neumayr & Uhlig, 1881 Scarburgiceras Buckman, 1924 — n Reineckeia Bayle, 1878 = Stenocadoceras Imlay, 1953 [e] Kepplerites Neumayr & Uhlig, 1892 , 8 K Grossouvria Siemiradzki, 1898 | Cranocephalites Spath, 1932 T N 1 d E d í N Lilloetia Crickmay, 1930 5 4 3 7 ^ Stephanoceras Waagen, 1869 o T * 3 Sonninia Bayle, 1879 N 3 | N Arkelloceras Frebold, 1957 2 Normannites Munier-Chalmas, 2 = H * 7 Tmetoceras Buckman, 1892 ? 5 1 — "Tr ii E m | Calpionellids ES E E Don a E a. * m 12 assemblage (see Pessagno and Blome, 1980; Blome, 1984a). However, the fact that Carter (written com- mun., 1985) recorded Parvicingula Pessagno, 1977a (sensu Pessagno and Whalen, 1982) in the middle Toarcian portion of the Maude Formation suggests BULLETIN 326 that this portion of Wrangellia was at Northern Teth- yan paleolatitudes by the middle Toarcian. In the following stratigraphic summary, we discuss only those formational units that bear Radiolaria de- scribed in Systematic Paleontology. T 120° PRINEVILLE 2 ^ N Lem CROOKED y (RIVER HWY. KAZEN kaso T 119° A \ SUPLEE-IZEE | AREA ,^ dë A I k Y MAP AREA A Se e | C \ EC HARNEY SCALE | o 10 20 INDEX MAP OF OREGON 109 BASIN 1188 MILES a A T T T 132* 131° COLANGARA 1 DIXON ENTRANCE B 54° 54° = Q GRAHAM | N ISLAND e : | T ^ E ÁKIDEGATE INLET 2 3 $ SANDSPIT A cz MAUDE |. ^ > H 53° 2 53° -= LOUISE | O AKUNGA | % o | Së ISLAND LYELL k * c LER l. ---- PHYSIOGRAPHIC BOUNDARY KUNGHIT |. SCALE [3 0 10 20 $ 52° — MILES d? 133° 132° (ld 1 1 ۱ A —Location of the Suplee-Izee area of Dickinson and Vigrass (1965) and adjoining areas in east-central Oregon; B—Index map of the Queen Charlotte Islands, British Columbia (from Pessagno and Blome, 1980). Text-figure 4. — Maps showing some of the localities described in this report. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 13 Stratigraphic Summary Kunga Formation The Kunga Formation (Sutherland Brown and Jef- frey, 1960; Sutherland Brown, 1968) consists of sili- ceous mudstone (“argillite”), limestone, and sand- stone. It rests comformably(?) on the Karmutsen Formation (Ladinian to Karnian) and either conform- ably beneath the Maude Formation (late Sinemurian?; early Pliensbachian to Toarcian) or unconformably be- neath the Yakoun Formation (Middle Jurassic). Sutherland Brown (1968, p. 51) divided the Kunga Formation into three informal members: (1) a lower massive gray limestone member that conformably(?) overlies the tholeiitic basalts (greenstones) of the Kar- mutsen Formation; (2) a middle, thin-bedded black limestone member; and (3) an upper thin-bedded black argillite member. The lower member is characterized by massive, gray-weathering recrystallized limestone with poorly-preserved corals, pelecypods, and am- monites. The only biostratigraphically significant fos- sils are rare Halobia sp. and Arcestes(?) sp. According to Sutherland Brown (1968, p. 61) the lower limestone member is Karnian, older than the Tropites welleri Zone.” At the type locality of the Kunga Formation at Kunga Island this unit is 183 m (600 ft) thick. The middle black limestone member includes predomi- nantly thin-bedded, flaggy, black, carbonaceous, mi- critic black limestone with lesser amounts of cross- bedded calcarenite, fine limestone conglomerate, black siliceous mudstone (““argillite”), and rare lithic sand- stone. At Kunga Island the middle member is 267 m (905 ft) thick. The middle member contains common but poorly-preserved pectenacids and rare ammonites. Monotis subcircularis Gabb, 1864, was recorded by both Sutherland Brown (1968) and Blome (1984a) in the upper part of this unit. The molluscan assemblage indicates that this member ranges in age from late early Karnian at its base to latest Norian at its top. Blome (1983, 1984a) recovered abundant well-preserved Ra- diolaria from the uppermost (upper Norian) part of the middle member and assigned this assemblage to the Betraccium Zone, B. deweveri Subzone. The upper black argillite member is characterized by thin, often rhythmically bedded black siliceous mudstone (“ar- gillite”), which superficially resembles ribbon chert. Minor lithic types include black, thin-bedded, micritic limestone, gray bioclastic limestone, dark-gray to greenish-gray lithic sandstone, and thin-bedded, black, calcareous shale. At Kunga Island the upper member is 497 m (1630 ft) thick. Sinemurian arietitid ammo- nites (e.g., Arietites Waagen, 1869) occur in all but the lower 56 m (184 ft) of the upper member. The lower interval between the last occurrence of Monotis sub- circularis Gabb, 1864, at the top of the middle member and the first occurrence of Sinemurian ammonites con- tains a rich, well-preserved radiolarian assemblage that is considerably different from that of the overlying Si- nemurian and radically different from that of the un- derlying upper Norian. It contains some elements, such as Canoptum merum Pessagno and Whalen, 1982, and Pantanellium kluense Pessagno and Blome, 1980, that also occur in the Graylock Formation (Hettangian) of east-central Oregon. Neither of these taxa has been observed either in the underlying latest Norian strata with Monotis subcircularis or in overlying Sinemurian strata with Arietites. Maude Formation The Maude Formation (MacKenzie, 1966; Suther- land Brown, 1968) includes dark-gray to black shale, siliceous mudstone (“argillite”), limestone, siltstone, and lithic sandstone. Bedded limestone and limestone nodules (black micrites) with abundant Radiolaria are common to abundant throughout most of the unit. The Maude Formation conformably overlies the Kunga Formation and disconformably(?) underlies the Ya- koun Formation (Middle Jurassic). Sutherland Brown (1968, p. 61) indicated that the Maude Formation reaches a maximum thickness of 183 to 213 m (600 to 700 ft). He stated, basing his conclusions on those of Frebold (1970), that the Maude Formation at its type locality at Maude Island ranges in age from late Sinemurian to Toarcian. The late Sinemurian age is questionable at least at the type locality in that Frebold (in Sutherland Brown, 1968, p. 65) indicated that both late Sinemurian and early Pliensbachian ammonites occur in the same one-foot bed in the lower part of the Maude. Detailed stratigraphic studies in progress by Dr. Howard Tipper and Mr. Bruce Cameron (Geolog- ical Survey of Canada) should resolve this problem. BLUE MOUNTAINS PROVINCE OF NORTHEAST AND EAST-CENTRAL OREGON The Blue Mountains Province contains four major tectonostratigraphic terranes that crop out discontin- uously in northeast-southwest trending belts beneath a Cenozoic volcanic cover (Dickinson, 1979). From northeast to southwest these terranes are the Seven Devils terrane, the Central melange terrane, the Me- sozoic clastic terrane, and the Huntington arc terrane (Dickinson, 1979; see Text-fig. 1). Many of the radi- olarian-bearing samples utilized in the present study are derived from part (Suplee-Izee area) of the Me- sozoic clastic terrane. 14 BULLETIN 326 A detailed discussion of the aforementioned terranes was presented by Pessagno and Blome (1986). Some of their conclusions are as follows: (1) The Seven Devils terrane, Central melange ter- rane, and Huntington arc terrane all represent dis- membered components of a single island-arc complex. (2) Faunal data from the Seven Devils, Mesozoic clastic, and Huntington arc terranes demonstrate that these terranes all resided in the Central Tethyan Prov- ince during the Late Paleozoic, Triassic, and most of the Early Jurassic; in the Northern Tethyan Province from the middle Toarcian (Early Jurassic) to the latest Bajocian (Middle Jurassic); in the Southern Boreal Province during the Bathonian and Callovian (Middle Jurassic); and at possible higher Boreal latitudes during the early Oxfordian (Late Jurassic). The shift from the Central Tethyan to Northern Tethyan Province is re- flected by the appearance of Parvicingula Pessagno, 1977a (sensu Pessagno and Whalen, 1982) in the mid- dle and late Toarcian strata of the Snowshoe Forma- tion (Warm Springs Member, Mesozoic clastic terrane, Suplee-Izee area). The shift from the Northern Te- thyan Province to the Southern Boreal Province is marked by a dramatic drop in pantanelliid diversity and abundance between the late Bajocian and late Bathonian (Mesozoic clastic terrane). There is a con- tinual drop in pantanelliid diversity from the early Bajocian (= middle Bajocian of Imlay, 1973, and Pes- sagno and Blome, 1980) onwards. More than twenty species-level taxa (named and unnamed forms) are present in the Aalenian and lower Bajocian; seven are present in the upper Bajocian (upper part of Mega- sphaeroceras rotundum Zone of Hall and Westermann, 1980); two are present in the upper Bathonian (= lower Callovian of Imlay, 1964a, and Pessagno and Blome, 1980); and one is present in the Callovian. A drop in diversity is also reflected in the ammonite assemblage between the late Bajocian and late Bathonian and Cal- lovian (see Imlay, 1973, 1981). In addition, the am- monite assemblage contains a predominance of Boreal Bathonian and Callovian genera such as Torricelliceras Buckman, 1922, Kepplerites Neumayr and Uhlig, 1892, and Pseudocadoceras Buckman, 1918. Missing are Cal- lovian Tethyan taxa such as Reineckeia Bayle, 1878, which, exclusive of the Circum-Pacific area of suspect and displaced terranes, occurs in east-central Mexico (Cantu Chapa, 1971; Imlay, 1980; Taylor et al., 1984), North Africa, and in the alpine-Himalayan belt (Ar- kell, Kummel, and Wright, 1957). (3) A Central Tethyan origin for the terranes of the Blue Mountains Province is not inconsistent with ex- isting paleomagnetic data. Hillhouse, Gromme, and Vallier (1982) indicated that the Seven Devils and Huntington arc terranes were situated 18? (+4°) north or south of the Triassic paleoequator. (4) The presence of Weyla Boehm, 1922, and Pli- catostylus Lupher and Packard, 1930, in Lower Juras- sic strata, and ammonites such as Lupherites Imlay, 1973, in Middle Jurassic strata (Mesozoic clastic ter- rane) suggests that the Blue Mountains island arc com- plex originated in the eastern Pacific (Pessagno and Blome, 1986; Smith, 1980; Westermann, 1981; Taylor et al., 1984). (5) Movement ofthe Blue Mountains island arc com- plex to Boreal latitudes is coincident with the opening of the Gulf of Mexico during the late Bathonian or Callovian (Pessagno and Blome, 1986). It is likely that the Blue Mountains island arc complex was carried to higher latitudes along megashear systems that are ge- netically related to those in Mexico (see Longoria, 1984, 1985). Stratigraphic Summary, Suplee-Izee Area (Mesozoic clastic terrane) The stratigraphic summary provided below only in- cludes radiolarian-bearing lithostratigraphic units mentioned in Systematic Paleontology. No attempt is made to describe the entire succession of the Suplee- Izee area and adjoining areas within the Mesozoic clas- tic terrane. Nicely Formation The Nicely Formation (Lupher, 1941; Dickinson and Vigrass, 1965; Imlay, 1968) consists of 23 m to 91 m (75-300 ft) of dark-gray, silty shales and mudstones often typified by an abundance of variable-sized dark- gray to black, micritic limestone nodules. The lime- stone nodules frequently contain megafossils and abundant Radiolaria. The Nicely Formation rests conformably upon the Suplee Formation (upper Sinemurian?, lower Pliens- bachian?; upper Pliensbachian) and beneath the Hyde Formation (upper Pliensbachian to middle Toarcian). Investigations of the Nicely ammonite fauna by Imlay (1968, pp. C8-C9) indicate that it is correlative with both the European Amaltheus margaritatus and Pleu- roceras spinatum Standard Zones of the upper Pliens- bachian. Hyde Formation The Hyde Formation (Lupher, 1941; Dickinson and Vigrass, 1965) includes 305 m (1000 to 1200 ft) of massive, blue-gray andesitic tuff and tuffaceous vol- canic wacke (turbidite). Thinner beds of tuffaceous mudstone with dark-gray limestone nodules occur at some horizons. The Hyde Formation rests conform- JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 15 ably beneath the Warm Springs Member of the Snow- shoe Formation (see below). Megafossils are rare and fragmentary in the Hyde Formation. However, Radiolaria are abundant at some horizons and commonly are well-preserved in the finer- grained clastics and limestone nodules. The age of the Hyde can only be established by superposition. It rests above Nicely strata bearing late Pliensbachian am- monites and below Snowshoe strata bearing late Toar- cian ammonites. Most of the unit is probably early Toarcian; however, it may well include late Pliens- bachian strata at its base and middle Toarcian strata at its top. Future studies of the radiolarian assemblage offer the best opportunity to determine the age of this unit. Snowshoe Formation The Snowshoe Formation (Lupher, 1941; Dickinson and Vigrass, 1965) in its type area at Izee (Text-fig. 1) includes 838 m (2750 ft) of dark-gray to black mud- stone, shale, volcaniclastic siltstone, tuff breccia, and volcaniclastic sandstone. Micritic, dark-gray to black limestone nodules containing abundant, well-pre- served Radiolaria occur in the finer-grained clastics. In its type area Dickinson and Vigrass (1965) subdi- vided the Snowshoe Formation into a lower member, a middle member, and an upper member. More re- cently, Smith (1980, pp. 1603-1608) applied the names “Warm Springs Member”, “Schoolhouse Member”, and “South Fork Member” to these same units (see below). To the east and west of the type area at Izee, the Schoolhouse Member interfingers respectively with the tuff, volcaniclastic sandstone, and tuff breccia of the Silvies Member and the Basey Member (see Dick- inson and Vigrass, 1965). The Snowshoe Formation rests conformably on the Hyde Formation and either conformably or unconformably beneath the Trow- bridge Formation (upper Bathonian to lower Callov- ian). The combined radiolarian and ammonite bio- Stratigraphic data indicate that the Snowshoe Formation in its type area near Izee ranges in age from middle Toarcian at its base to late Bathonian at its top (Imlay, 1981; see loc. OR-589 in Appendix). Warm Springs Member. The Warm Springs Mem- ber (Lupher, 1941; Dickinson and Vigrass, 1965; Smith, 1980) consists of 140 to 200 m (459 to 656 ft) of reddish-brown weathering, black to dark-gray mud- stone, fissile shale, and siltstone. Lenticular masses of micritic to silty limestone and common micritic, dark- gray limestone nodules are common at most localities. Ammonites frequently occur in the limestone nodules and finer-grained clastics. Abundant Radiolaria occur in the limestone nodules. The contact of the Warm Springs Member with the volcanic wacke of the un- derlying Hyde Formation is conformable and may be either sharp or gradational in the area near Izee (Text- fig. 4). Radiolarian and ammonite data indicate that the Warm Springs Member ranges in age from middle Toarcian to early Bajocian (Imlay, 1973; see loc. OR- 589 in Appendix for Toarcian data). At Schoolhouse Gulch immediately north of Lee (Text-fig. 4), the lower 26.8 m (88 ft) of the Warm Springs Member are as- signable to the middle and upper Toarcian (= thouars- ense, variabilis, and levesquei Standard Zones). The remainder of the Warm Springs Member near Izee is assignable to the Aalenian (= lower Bajocian of Imlay, 1973; Pessagno and Blome, 1980; Pessagno and Wha- len, 1982) and lower Bajocian (= middle Bajocian of Imlay, 1973). Aalenian strata contain Tmetoceras Buckman, 1892, and Eudmetoceras Buckman, 1920, and are placed by Imlay (1980, p. 23) in the middle and upper Aalenian. Evidence for the lower Aalenian opalinum Standard Zone is lacking (Hall and Wester- mann, 1980). Lower Bajocian Warm Springs strata contain ammonites that are correlative with the stan- dard European discites, laeviuscula, sauzei, and hum- phriesianum Standard Zones (Smith, 1980, p. 1606). Smith indicates that the upper part of the Warm Springs Member decreases in age from southwest to northeast. Schoolhouse Member.—The Schoolhouse Member in its type area near Izee consists of 300 m (984 ft) of laminated, gray, green, and rarely buff-colored siltstone and sandstone that alternate with mudstone and shale similar to those of the Warm Springs Member. Lam- inae range in thickness from 1 mm to 1 cm (Smith, 1980, p. 1605). Dickinson and Vigrass (1965) indicate that the coarser layers are graded and consist mostly of andesitic plagioclase and rock fragments, which were originally glassy but now are zeolitized. The School- house Member conformably overlies the Warm Springs Member and rests conformably beneath the South Fork Member. The Schoolhouse Member contains a lower to upper Bajocian ammonite assemblage (Imlay, 1973; Smith, 1980), which is correlated with the European /aevius- cula, sauzei, humphriesianum, and subfurcatum Stan- dard Zones. Smith (1980, p. 1607) indicated that the lower part of the Schoolhouse Member to the northeast at Bunton Hollow is younger than the upper part of the unit to the southwest at Flat Creek and Pole Can- yon. South Fork Member.—The South Fork Member (Dickinson and Vigrass, 1965, p. 47; Smith, 1980, p. 1605) consists of over 500 m (1640 ft) of dark-gray to 16 BULLETIN 326 black shale and mudstone, with gray calcareous, partly volcaniclastic sandstone, which rests conformably on the Schoolhouse Member and either conformably (e.g., near Izee) or unconformably (Loc. OR-513 [see Ap- pendix]) beneath the Trowbridge Formation (upper Bathonian(?); lower Callovian). The graded nature of the sandstone strata suggests that they are turbidites (Smith, 1980, p. 1605). The South Fork Member thins from northeast to southwest. At Pole Canyon and at Flat Creek to the southwest of Izee and south of the South Fork of the John Day River, the South Fork Member is missing due to erosion (Text-fig. 4). In this case, the Trowbridge Formation rests unconformably on the Schoolhouse Member. The lower part of the South Fork Member in the Izee area contains upper Bajocian ammonites that are correlative with the Eu- ropean subfurcatum Standard Zone and the American Megasphaeroceras rotundum Zone (Smith, 1980, pp. 1606-1607). Upper Bathonian ammonites have been reported by Imlay (1981, p. 10) from the upper 183 to 213 m (600 to 700 ft) of the South Fork Member along Rosebud Gulch north of Izee. Lonesome Formation The Lonesome Formation (Lupher, 1941; Dickin- son and Vigrass, 1965) includes approximately 3050 m (10,000 ft) of monotonous, flysch-like interbedded gray, graded sandstone and dark-gray mudstone typi- cally exposed on the South Fork of the John Day River southeast of Izee (Text-fig. 4). This unit rests conform- ably on the dark-gray, black, and often green tuffaceous shale and sandstone of the Trowbridge Formation (lat- est Bathonian to early Callovian) and unconformably beneath Tertiary volcanic rocks (Dickinson and Vi- grass, 1965). Imlay’s (1981) recent revision of the am- monite biostratigraphy indicates that the Lonesome Formation is of early and early middle Callovian age. To date, only sparse (silicified and calcified) Radiolaria have been recovered from this unit (Pessagno and Blome, 1980; Pessagno and Whalen, 1982; Pessagno and Blome, 1982; Blome 1984b). THE COAST RANGE OPHIOLITE AND ASSOCIATED STRATA California Coast Ranges The genesis of the Coast Range ophiolite and its associated sedimentary strata has been discussed in detail by Hopson, Mattinson, and Pessagno (1981). A revision of the chronostratigraphy and radiolarian bio- stratigraphy was presented by Pessagno, Blome, and Longoria (1984). From earlier and current analyses of these rocks, the following facts are evident: (1) Strata associated with pillow basalts within the Coast Range ophiolite are invariably red, manganifer- ous radiolarian cherts and minor pelagic limestones lacking tuffaceous (calc-alkaline) contributions. The red ribbon cherts are identical to those that characterize the Franciscan Complex. Their presence within the ophiolite at numerous localities indicates that the spreading center for the Coast Range ophiolite was not in the immediate vicinity of an island arc at the time when oceanic crust was being generated. (2) Strata overlying the Coast Range ophiolite at all localities are always green to black tuffaceous chert, tuff, tuff breccia, and occasional lenses and beds of light-gray pelagic limestone. (3) U/Pb dates of the Coast Range ophiolite range in age from 153 + 3 m.y. at Cuesta Ridge (San Luis Obispo Co.), 161 + 3 m.y. at Point Sal (Santa Barbara Co.), 156 + 3 m.y. at Arroyo del Puerto (Stanislaus Co.), and 164 + 3 m.y. at Llanada (San Benito Co.) (see Hopson, Mattinson, and Pessagno, 1981). Ac- cording to Hopson, Mattinson, and Pessagno (1981, p. 466), Deborah Fritz (Univ. of Texas at Austin) re- ported a 163 + 5 m.y. K/Ar age on the Paskenta rem- nant (Tehama Co.) of the Coast Range ophiolite. (4) In Northern Tethyan strata in eastern Mexico (Taman Formation) and in Southern Boreal strata in the California Coast Ranges, Zone 2 (sensu Pessagno, Blome, and Longoria, 1984) can be divided into an upper portion whose base is marked by the first oc- currence of Parvicingula Pessagno, 1977a, s. s. and a lower portion characterized by the presence of Parvi- cingula s. l. Parvicingula s. s. includes forms (e.g., P. santabarbaraensis Pessagno, 19772) that possess a long, slender, yet sturdy tube on the final post-abdominal chamber; Parvicingula s. l. includes forms (e.g., P. pro- funda Pessagno and Whalen, 1982; P. vera Pessagno and Whalen, 1982) that lack the post-abdominal ap- paratus. If Parvicingula s. l. possesses a post-abdom- inal tube, it is most likely quite broad and fragile, and similar to that of Canoptum Pessagno, 1979. In east-central Mexico (San Luis Potosí) Parvicin- gula s. s. first appears well above the base of the Glo- chiceras gp. fialar Zone (upper Kimmeridgian sensu gallico*, Cantu Chapa, 1971) in the upper part of the lower member of the Taman Formation. However, it cannot be determined at present whether Parvicingula s. s. first appears in the uppermost part of the G. gp. fialar Zone (uppermost Kimmeridgian) or in the low- ermost part of the overlying Virgatosphinctes mexi- canus-Aulacomyella neogeae Zone (lowermost Ti- thonian). In the California Coast Ranges, Parvicingula s. S. first appears in the volcano-pelagic succession at * This qualification was suggested by Westermann (written com- mun., 1984) to distinguish French from English views on the subject. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 17 Point Sal (Santa Barbara Co.; Hopson, Mattinson, and Pessagno, 1981, loc. 2) between 10.6 m (35 ft) and 11.5 m (38 ft) above the contact with the Coast Range ophiolite. Near Paskenta (Tehama Co.; Hopson, Mat- tinson, and Pessagno, 1981, loc. 22), Parvicingula s. s. occurs in upper Zone 2 strata (Great Valley Super- group?) overlying the ophiolite breccia unit, which in turn overlies the Coast Range ophiolite. At this local- ity, Parvicingula s. s. is directly associated with Buchia rugosa (Fischer, 1830-1837) and forms transitional to B. concentrica (Sowerby, 1827). Both Jones (1975, p. 330) and Imlay (1980, p. 63) favored assigning the Strata bearing Buchia Rouillier, 1845, to the upper Kimmeridgian. However, Imlay indicated that these strata might also be assignable to the lower Tithonian. Significantly, Lanphere (1971, p. 3210) obtained a K/Ar date of 151 + 5 m.y. ata nearby locality from a diabase dike intruding the Coast Range ophiolite, but intruding neither the ophiolite breccia unit nor the overlying strata bearing Parvicingula s. s. and Buchia rugosa. The Decade of North American 1983 Geologic Time Scale (Palmer, 1983; Kent and Gradstein, 1985) placed the Kimmeridgian-Tithonian boundary at 152 + 12 m.y. Harland et al. (1982) placed the Kimmeridgian- Tithonian boundary at 150 Ma. The data presented above suggest that the Kimmeridgian-Tithonian boundary is younger than 151 m.y. and probably should be placed at 150 Ma as suggested by Harland et al. Pessagno, Blome, and Longoria (1984) concluded from their analysis of biostratigraphic data from North America, the Deep Sea Drilling Project, the Mediter- ranean area, and Rumania that the base of Zone 2 (= first occurrence of Mirifusus Pessagno, 1977a) occurs in strata equivalent to the divisum Standard Zone (up- per lower Kimmeridgian) or to the acanthicum Stan- dard Zone (lower upper Kimmeridgian) of the Euro- pean Tethyan Realm. Recent studies by Pessagno and Blome demonstrate that the Zone 1-Zone 2 boundary now can be recognized in the Klamath Mountains of northwestern California (Western Klamath terrane, Smith River subterrane; Harper, 1983, loc. 1). At Har- per locality 1 the Galice Formation s. /. rests on the Josephine ophiolite. Well-preserved, abundant upper Zone 1 Radiolaria were recovered from the Galice For- mation at 3.2 m (10.5 ft) and 12.8 m (42 ft) above the sedimentary contact with the Josephine ophiolite. Lower Zone 2 Radiolaria were recovered from samples 17.5 m (58 ft) to 61.2 m (201 ft) above the contact with the ophiolite. Moreover, Saleeby et al. (1982) obtained a concordant U/Pb date of 157 + 2 m.y. (on zircon) from plagiogranite within the Josephine ophiolite. In addition, these workers also obtained a concordant U/Pb date of 150 + 2 m.y. (on zircon) from a keratophyre sill intruding the Galice Forma- tion. The geochronometric data cited above establish that the Zone 1-Zone 2 boundary is younger than 157 Ma and older than 150 Ma. It should be noted that only Central Tethyan Radiolaria have been observed in the lower 17.5 m (58 ft) of this succession. However, Southern Boreal Radiolaria were recovered from sam- ples 54 m (178 ft) to 61 m (201 ft) above the contact with the Josephine ophiolite. The 157 Ma date on the Josephine ophiolite is sig- nificant in that it can be related to ammonite and bi- valve biostratigraphic data as well as U/Pb geochro- nometric data from the nearby Rogue Valley subterrane (Western Klamath terrane) of southwestern Oregon. In the Rogue Valley subterrane Saleeby (1984) obtained a concordant U/Pb date of 157 + 2 m.y. (on zircon) from dacitic tuff breccia in the upper several hundred meters of the Rogue Formation. Moreover, Imlay (1961) recovered the middle Oxfordian ammonite Di- chotomosphinctes Buckman, 1926, from the lower part of the overlying Galice Formation s. s. in the same area. In the Submediterranean Province (European Tethyan Realm), Meléndez, Sequeiros, and Broch- wicz-Lewinski (1984) demonstrated that Dichotomo- sphinctes ranges from the antecedens Standard Zone (rotoides Standard Subzone) to the transversarium Standard Zone (schilli Standard Subzone). We follow Zeiss (Enay and Meléndez, 1984, table 4) in assigning the antecedens Standard Zone to the lower middle Ox- fordian and the schilli Standard Subzone to the middle part of the middle Oxfordian. Dichotomosphinctes is also associated with Buchia concentrica (Sowerby, 1827) in the lower part of the Galice. Imlay (1955, 1961, 1980) established that in North America, B. con- centrica does not range below the first occurrence of Amoeboceras Hyatt, 1900. In addition, Imlay (1961, p. D-11) noted that in the Naknek Formation of Alas- ka, B. concentrica is associated with both Amoeboceras and Dichotomosphinctes. Sykes and Callomon (1979) established that Amoeboceras does not range below the base of the glosense Standard Zone (ilovaiskii Standard Subzone) in Great Britain (Boreal Realm). Further- more, Zeiss (in Enay and Meléndez, 1984, table 4) tentatively correlated the Boreal ilovaiskii Standard Subzone with the Tethyan schilli Standard Subzone. It is apparent that this correlation is strengthened by the association of Amoeboceras and Dichotomo- sphinctes in the Naknek Formation of Alaska. The concurrence of Dichotomosphinctes and B. concentrica in the lower part of the Galice Formation demonstrates that this interval should be assigned to the middle part of the middle Oxfordian. The combined biostrati- graphic and geochronometric data from the Rogue For- mation and overlying Galice Formation therefore in- dicate that the middle part of the middle Oxfordian is younger than 157 Ma. Moreover, these data indicate that the 156 Ma age for the Oxfordian-Kimmeridgian boundary advocated by Kent and Gradstein (1985) is too old. Westermann (1984) used what he termed the “scaled equal subzone method” to calculate the rela- tive duration of Jurassic standard ammonite zones. He concluded that the middle Oxfordian represented 1.7 Ma and that the upper Oxfordian represented 2.6 Ma. If the Oxfordian—Kimmeridgian boundary is placed at 156 Maas suggested by Kent and Gradstein, more than one third of Oxfordian time would be crowded into less than 1 million years. (5) The high TiO, values of basalts associated with ophiolite-like masses at Stoneyford and Wilbur Springs indicate that these rocks are representative of ocean island basalts and are beyond the compositional range of ocean ridge basalts (Hopson, Mattinson, and Pes- sagno, 1981; Hopson, oral commun., 1983). (6) Immediately noticeable in the upper half to one- third of Upper Jurassic volcano-pelagic successions above the Coast Range ophiolite (e.g., Point Sal and Stanley Mountain) and in the overlying Great Valley Supergroup are the abundance and diversity of species of Parvicingula Pessagno, 1977a, and the low diversity of pantanelliids (see East-central Mexico herein). This evidence together with the abundance of Buchia Rouil- lier, 1845, in the Great Valley Supergroup indicates that these strata were deposited in the Boreal Realm (Text-figs. 2, 3). Imlay and Jones (1970, p. 319) indi- cated that the Upper Jurassic (upper Tithonian, sensu Pessagno, Blome, and Longoria, 1984) ammonite as- semblage of the Great Valley Supergroup displays very strong “southern or Mediterranean” affinities. How- ever, they noted that the Buchia are much more com- mon numerically than the ammonites and are clearly indicative of a northern (Boreal) derivation. We con- clude, therefore, that the upper half to one-third of the volcanogenic-pelagic succession above the Coast Range ophiolite as well as all of the overlying Great Valley Supergroup was deposited at latitudes within the Southern Boreal Province (Text-fig. 3). In contrast, the red (non-tuffaceous), manganiferous, radiolarian-bear- ing ribbon cherts that are interbedded with the ophio- lite at Point Sal (Santa Barbara Co.), Llanada (San Benito Co.), and Paskenta (Tehama Co.) are Tethyan (Central Tethyan). At most localities these cherts are recrystallized and the radiolarians poorly preserved. However, at Paskenta a sample submitted in 1973 to the senior author by Deborah Fritz (Univ. of Texas at Austin) was found to contain a diversified, moderately well-preserved late Callovian to Oxfordian (upper Zone 1) fauna. Significantly, the nassellarian assemblage lacks Parvicingula Pessagno, 1977a (sensu Pessagno and Whalen, 1982) but contains abundant specimens of BULLETIN 326 Ristola Pessagno and Whalen, 1982; pantanelliids, though present, are poorly preserved. The abundance of Ristola, together with the lack of Parvicingula, dem- onstrates that this assemblage is representative of the Central Tethyan Province (Text-fig. 2). As noted pre- viously, the red ribbon cherts of the Franciscan Com- plex (Lower Jurassic to Upper Cretaceous) likewise contain a Tethyan—dominantly Central Tethyan—ra- diolarian assemblage. (7) Paleomagnetic data on the Coast Range ophiolite are presently sparse. However, McWilliams and How- ell (1982, p. 215) determined that the ophiolite (pillow basalts) at Stanley Mountain (Alamo Canyon, San Luis Obispo Co.) originated at 14° + 7 north or south of the Middle to Late Jurassic paleoequator. The over- lying volcanogenic-pelagic succession at this locality is 103 m (338 ft) thick (Hopson, Mattinson, and Pessag- no, 1981; Pessagno, Blome, and Longoria, 1984). In- vestigations by Pessagno and Blome indicate that the lower 61 m (199 ft) of this section contain a Central Tethyan Zone 2 (upper Oxfordian?; Kimmeridgian, sensu gallico) fauna composed of Ristola Pessagno and Whalen, 1982, and, when well-preserved, a diversified pantanelliid assemblage. These investigations indicate further that the lower part of Zone 3 and possibly the upper portion of Zone 2 (sensu Pessagno, Blome, and Longoria, 1984) are missing. The interval from 62 m (204.5 ft) to below 73 m (239 ft) likewise contains a Central Tethyan upper Zone 3 (lower Tithonian) as- semblage still rich in Ristola, but totally lacking Par- vicingula Pessagno, 1977a; sensu Pessagno and Wha- len, 1982. Samples from 73 m (239 ft) contain Parvicingula and poorly-preserved pantanelliids; these samples may be assignable to either the Northern Teth- yan Province or to the Southern Boreal Province (Text- fig. 2). The interval from 80 m (261 ft) to the top of the section contains a Parvicingula-rich Southern Bo- real assemblage assignable to upper Zone 3 (lower Ti- thonian) and to lower Zone 4 (basal upper Tithonian, sensu Pessagno, Blome, and Longoria, 1984). Well- preserved radiolarian faunas from pelagic limestones at 80 m (261 ft; Zone 3) and 101 m (330 ft; Zone 4) contain poorly-diversified pantanelliids (two or three species-level taxa; see East-central Mexico herein). At Point Sal the volcanogenic-pelagic succession above the Coast Range ophiolite is only 23+ m (75+ ft) thick. Below 11 m (35 ft), the strata are somewhat recrystallized and the faunas are generally not spec- tacular. Sparse Central Tethyan upper Zone 1 faunas (Oxfordian to lower Kimmeridgian, sensu gallico) con- taining Ristola and lacking Parvicingula occur in the lower 4 m (14 ft) of the succession above the contact with the ophiolite. Central Tethyan Zone 2 faunas oc- cur at 4.5 m (15 ft) and 5 m (18 ft). A sample (loc. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 19 NSF-906) from 11 m (35 ft) assignable to lower Zone 2 (upper portion; upper Kimmeridgian) contains Par- vicingula s. L, no Parvicingula s. s., and poorly-pre- served pantanelliids. This sample may be representa- tive of either the Northern Tethyan Province or the Southern Boreal Province. However, upper Kimmer- idgian (upper Zone 2) and lower Tithonian samples (Zone 3) from 11.5 m (38 ft) and above contain definite Southern Boreal faunas. Because many of these sam- ples (e.g., locs. NSF-907, NSF-908, and NSF-909; see Appendix) contain well-preserved Radiolaria derived from pelagic limestone, there can be little doubt about the low diversity of the pantanelliid assemblage or the high diversity of the Parvicingula assemblage (with Parvicingula s. s.). EAST-CENTRAL MEXICO This area lies approximately between the latitude of Tampico to the north and Veracruz to the south. It includes an Upper Jurassic and Lower Cretaceous bathyal succession that has a direct bearing on the opening of the Gulf of Mexico, in that it lies astride the axis of sea floor spreading and rifting shown by Buffer et al. (1980) for the Gulf of Mexico. This deep- water segment of the Sierra Madre Oriental, referred to by Longoria (1984) as the Huayacocotla segment, is flanked to the north and south by shelf deposits characterized by evaporites and carbonates. Upper Ju- rassic formational units within the Huayacocotla seg- ment of the Sierra Madre Oriental are characterized by the association of ammonites, ammonite aptychi, pectenacids, abundant Radiolaria, calpionellids, and nannoconids. The presence of calpionellids together with a molluscan assemblage of strong Mediterranean affinities indicates that this region was part ofthe Teth- yan Realm (see Cantu Chapa, 1971; Imlay, 1980, p. 38). The radiolarian assemblage is characterized by the presence of Parvicingula Pessagno, 1977a (sensu Pes- sagno and Whalen, 1982), and by an abundant diver- sified assemblage of pantanelliids. Species of Panta- nelliidae (Pessagno, 1977b; Pessagno and Blome, 1980) are considerably more abundant and diversified in the Taman Formation than they are in strata of Kimmer- idgian or Tithonian age in the Boreal Realm (e.g., Gal- ice Formation, Northern California; volcanogenic-pe- lagic strata overlying the Coast Range ophiolite at Point Sal and Stanley Mountain). There are generally three to four times more species-level taxa present in the assemblage of the Taman Formation than there are in Boreal strata of the same age in California (Pessagno, Longoria, MacLeod, and Six [in press]). It also should be noted that the Taman Formation contains Tethyan Species (e.g., Acanthocircus dicranocanthos Squinabol, 1914), which never have been observed in the Boreal California assemblage. 4. dicranocanthos is a Central Tethyan and Northern Tethyan species that occurs in red ribbon cherts from the Mediterranean area, Oman, the East Indies, and the Franciscan Complex (Text-fig. 3). The radiolarian assemblage of east-central Mexico thus appears to link the assemblages of the Central Tethyan Province with those of the Southern Boreal Province. This together with the Tethyan nature of the megafossil assemblage indicates that this region is rep- resentative of the Northern Tethyan Province. Stratigraphic Summary Taman Formation The Taman Formation (Heim, 1926, pp. 84-89) in its type area at Taman (San Luis Potosi) includes thin- to medium-bedded, dark-gray to black, organic-rich, petroliferous micritic limestone with interbeds of black shale. Regionally, the Taman ranges in thickness from 200 m (656 ft) to 500 m (1640 ft). In its type area it can be subdivided into a lower unit comprised of pre- dominantly medium-bedded limestone with thin shale interbeds and an upper unit consisting of thin-bedded limestone commonly associated with thicker, buff- weathering black shale intervals (upper portion = low- er part of Pimienta Formation of Cantu Chapa, 1971). Limestone nodules are prevalent in the upper part of the lower member and in the upper member. The Ta- man Formation rests conformably on the black, com- monly phyllitic shale of the “Santiago” formation (Cal- lovian to Oxfordian) and beneath the thin-bedded chert, limestone, and tuff of the Pimienta Formation (upper Tithonian(?); Berriasian). The Taman Formation, as defined above in its type area, includes early Kimmeridgian to late Tithonian strata. It encompasses (in ascending order) the Atax- ioceras, Idoceras, Glochiceras gr. fialar, Virgato- sphinctes mexicanus—Aulacomyella neogeae, and Ma- zapilites zones of Cantu Chapa (1971) and radiolarian zones 1 (upper part), 2, 3, and 4 (lower part) (Pessagno, Blome, and Longoria, 1984). It should be noted that the base of Zone 4 (upper Tithonian) corresponds closely to the first occurrence of Crassicollaria inter- media (Durand Delga, 1957) and occurs below the top of the lower Taman in the Taman-Tamazunchale area (San Luis Potosi). According to Cantu Chapa (1971) the top of the V. mexicanus-A. neogeae Zone corre- sponds to the top of what we refer to as lower Taman (= Taman Formation and part of Pimienta Formation of Cantu Chapa, 1971) whereas the base of the Ma- zapilites Zone corresponds to the base of the upper Taman (= Pimienta Formation [in part] of Cantu Cha- pa, 1971). However, the senior author (May, 1985) collected Aulacomyella neogeae Imlay, 1940, 30 m 20 BULLETIN 326 (96.8 ft) above the contact between the lower and upper Taman at Barrio de Guadalupe (San Luis Potosi; loc. MX 85-35). It would appear, therefore, that the upper part of the V. mexicanus-A. neogeae Zone overlaps the lower part of the Mazapilites Zone. This and other problems pertaining to Cantu Chapa’s ammonite zo- nation for the Tithonian are discussed in detail by Pessagno, Longoria, MacLeod, and Six [in press]. VIZCAINO PENINSULA, BAJA CALIFORNIA SUR, MEXICO The geology of this complex area is still poorly known in spite of recent efforts by workers such as Barnes (1982). It is difficult to ascertain at the moment wheth- er or not displaced terranes are present in this region. The presence of common Buchia Rouillier, 1845, with- in the Eugenia Formation (upper Tithonian to Aptian) together with Boreal foraminiferal faunas in the over- lying Valle Formation (Albian to Turonian or younger) suggests that these strata were deposited within the Boreal Realm. Curiously, Upper Cretaceous plankton- ic foraminifera from the Valle Formation (Longoria, oral commun., 1983) are more similar to those de- scribed by Douglas (1969) from northern California than they are to those described by Bandy (195 1) and Sliter (1968) from southern California. Well-preserved Upper Jurassic and Cretaceous Radiolaria from the Eugenia and Asuncion formations (Davila, 1986) are quite similar to those described by Pessagno (1976, 1977a, 1977b) and by Pessagno, Blome, and Longoria (1984) from California, and are definitely Southern Boreal in aspect. In general, the radiolarian faunas are not as diversified as those from California. Further- more, a well-preserved late Pliensbachian radiolarian assemblage extracted from limestone in the sandstone member of the San Hipölito Formation (see below) is poorly diversified (including pantanelliids) and ap- pears to be more representative of the Boreal Realm. Radiolaria extracted from Upper Triassic cherts in the San Hipölito Formation are not as well preserved. However, many species present in the Karnian-Norian assemblage ofthe San Hipölito Formation are not rep- resented in coeval Tethyan strata in the Queen Char- lotte Islands and east-central Oregon (Pessagno, Finch, and Abbott, 1979; Pessagno and Blome, 1980; Blome, 1984a). Stratigraphic Summary San Hipölito Formation The San Hipölito Formation (Mina, 1957) at its type locality at Punta San Hipölito includes 2400 m (7848 ft) of section. Finch and Abbott (1977) divided the San Hipölito Formation into four informal members. In ascending order these are (1) a chert member; (2) a limestone member; (3) a breccia member; and (4) a sandstone member. The San Hipölito Formation rests conformably on pillow basalts (andesitic basalts?); the top of the unit is not exposed in the area around Punta San Hipölito. Triassic zonal terminology follows that of Blome (1984a). Chert Member. The chert member includes up to 245 m (801 ft) of green to red tuffaceous cherts with subordinate amounts of volcanic sandstone and con- glomerate. Pectenacids (e.g., Halobia Bronn, 1830) and abundant Radiolaria occur throughout much of this unit. Pessagno, Finch, and Abbott (1979) indicated that the lower 101 m (330 ft) of the chert member are assignable to the Capnodoce Zone (upper Karnian?; lower to upper middle Norian). The boundary between the overlying Betraccium Zone, Pantanellium silber- lingi Subzone (upper middle Norian; upper Norian?) occurs between 100.8 m (330 ft) and 114.2 m (373 ft). All but the uppermost 5 m (16 ft) of the upper 61 m (201 ft) of the chert member are assignable to the P. silberlingi Subzone. Limestone Member. — This unit includes up to 209 m (687 ft) of alternating beds of limestone and vol- caniclastic sandstone, which rest conformably on the chert member. Limestone predominates in the upper half of the limestone member, whereas sandstone pre- dominates in the lower half of the unit. Monotis sp. cf. M. subcircularis Gabb, 1864, has been identified by Dr. N. J. Silberling (U. S. Geological Survey, Denver, CO) from the uppermost part of the limestone mem- ber. Poorly-preserved calcified Radiolaria occur throughout the limestone member. Breccia Member.—The breccia member is a lentic- ular mass with a maximum thickness of 105 m (343 ft). It consists of large blocks of neritic limestone set ina matrix of volcanic litharenite. The breccia member rests disconformably on the limestone member. Lime- stone boulders contain corals, coralline algae, and ben- thonic foraminifera. No Radiolaria are presently known from this member. Because Upper Triassic Radiolaria occur in the basal portion of the sandstone member (see below), the breccia member can be assigned to the upper Norian. ۱ Sandstone Member. — According to Finch and Ab- bott (1977), the sandstone member has a maximum thickness of 1840 m (6017 ft) and consists of light-gray to brown, volcaniclastic sandstone and siltstone, tuff, conglomerate, and silty tuffaceous limestone. This unit rests conformably(?) on the underlying breccia mem- ber. No megafossils have been observed to date; how- ever, Radiolaria are abundant and well preserved in tuffaceous, bedded limestone strata and in limestone nodules. Whalen has recovered Upper Triassic Radi- JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 24 olaria 13 m (42 ft) and 19 m (62 ft) above the base of the sandstone member and Lower Jurassic (upper Pliensbachian, Toarcian?) Radiolaria were recovered from 300 m (984 ft) and 400 m (1312 ft) above the base of the sandstone member. SYSTEMATIC PALEONTOLOGY INTRODUCTION Pessagno, Blome, and Longoria (1984, p. 21) noted that there are radical differences in the concept of mor- phospecies among radiolarian specialists. They stated This, to a large degree, depends on whether on one is a Cenozoic or a Mesozoic specialist and furthermore, it appears to be related to the mode of illustrating and studying radiolarian taxa. Most Ceno- zoic Radiolaria have tests comprised of opaline silica. When spec- imens are properly cleaned, their internal and external features are readily discernible and can be easily illustrated using transmitted light optics. Few, if any, Mesozoic Radiolaria have tests comprised of opaline silica. Their tests, instead, have been replaced by quartz, chalcedony, smectite, pyrite, limonite, and calcite. Even specimens whose tests are still siliceous are often difficult to photograph with transmitted light optics simply because test walls are not sufficiently hyaline. Whereas transmitted light optics are still the primary tool of the Cenozoic specialist, the scanning electron microscope by necessity has become the primary tool of the Mesozoic specialist. Because the scanning electron microscope is capable of recording the minutest details of radiolarian morphology, students of Mesozoic Radiolaria are presented with a wealth of morphological data. Taxa are therefore described in more detail than would be normal utilizing transmitted light optics. As a result, Cenozoic specialists tend to be regarded by Mesozoic specialists as ultra ‘lumpers’ and most Mesozoic specialists are regarded by Cenozoic specialists as ultra ‘splitters’. Mesozoic and Cenozoic workers now agree that much of the classification utilized by Haeckel (1887) is highly artificial in character and needs to be replaced by a more phylogenetic classification (see Riedel, 1971; Pes- sagno, 1977c). Unfortunately, Haeckel’s classification was based largely on the geometry or shape of the radiolarian test. The senior author believes that to ob- tain a more phylogenetic classification one must con- sider how the radiolarian test is constructed. This is particularly pertinent at the family and superfamily levels. Such a thesis is reflected in reports by Pessagno (1973), Pessagno and Blome (1980), Baumgartner (1980a), Pessagno and Whalen (1982), and Blome (1983). Hopefully, it is reflected in this report (see Test Construction below). In this section the designation USNM indicates that a type specimen has been deposited at the U. S. Na- tional Museum of Natural History, Smithsonian In- stitution, Washington, DC, and has been assigned a catalogue number. Holotypes are isolated on one-hole cardboard slides bearing a USNM catalogue number; paratypes deposited at the U. S. National Museum are mounted in HYRAX* or CAEDAX** on a glass slide and also bear a USNM catalogue number. Paratypes deposited in the Pessagno Collection are isolated on one-hole cardboard slides. New taxa described in this report are illustrated by means of scanning electron micrographs. When pres- ervation permits, transmitted light photomicrographs are also utilized (see Pl. 11). Measurements are made with micrometers implant- ed in the oculars of either a stereoscopic microscope or a transmitted light microscope. All measurements have been converted from millimeters to um (1 um — ۱۵ ٩ eh, TEST CONSTRUCTION Two families, the Farcidae, n. fam., and the Hila- risiregidae Takemura and Nakaseko (1982), display cephalic skeletal elements that include the following components: primary and secondary left lateral bars; primary and secondary right lateral bars; vertical bar; and apical bar (Pl. 1, figs. 3, 11, 17, 18). Significantly, in both families the dorsal bar is absent (see Takemura and Nakaseko, 1982). The Ultranaporidae likewise have a similar array of cyrtoid cephalic skeletal ele- ments (Pl. 1, figs. 8, 15), but differ in possessing a dorsal bar. This latter arrangement is common to most Me- sozoic Nassellariina. The Farcidae and Hilarisiregidae appear to show an alignment of their four feet with the two primary lateral bars and two secondary lateral bars (Pl. 1, figs. 11, 17). There is no direct structural con- nection on most specimens between the feet and the opposing cephalic skeletal elements. The exception ap- pears to be one unusual specimen of the farcid genus Rolumbus, n. gen., which displays a direct connection between the primary and secondary lateral bars and the proximal extensions of the triradiate feet (Pl. 1, figs. 1, 16). In Hilarisirex Takemura and Nakaseko, 1982, one sees an alignment of the feet (Pl. 1, fig. 17) with the primary and secondary lateral bars. The feet are not connected directly to the cephalic skeletal ele- ments but are continuous with the sides of the A-frames (Pl. 1, figs. 13, 17). In the case of the Ultranaporidae Pessagno, 1977b, one foot of Napora Pessagno, 1977a, is aligned with the dorsal bar and the two remaining feet are aligned with the primary left lateral and right lateral bars. Many, but not all, species of Napora show an alignment of pore frames between the proximal portions of the feet and cephalic skeletal elements both internally and externally (e.g., Pl. 6, figs. 15, 20; Pl. 9, fig. 18). Where this lineation is visible externally, it * HYRAX is a product of Custom Research and Development, Auburn, CA. ** CAEDAX is a product of EM Laboratories, Elmsford, NY. 22 BULLETIN 326 appears to be directly aligned with the outermost lon- gitudinal ridges of a given triradiate foot. Jacus De Wever, 1982, displays the same sort of arrangement of cephalic skeletal elements and opposing feet dis- played by Napora. De Wever’s illustration of the in- terior of Jacus coronatus De Wever, 1982 (pl. 12, fig. 3) appears to indicate an alignment of pore frames. It is suggested here that the arrangement of cephalic skeletal elements noted above may serve as a template for test secretion, at least with monocyrtid, dicyrtid, and tricyrtid Nassellariina with prominent triradiate feet. This hypothesis needs to be tested, however, through the study of both fossil and Recent Radiolaria. Both the Farcidae, n. fam., and the Ultranaporidae Pessagno, 1977b, seem to share a method of pore frame secretion that ultimately results in test thickening. In viewing either the farcid or the ultranaporid test from its interior, one immediately notices that the pore frames are smooth and flattened with little or no relief (Pl. 1, figs. 12, 15; Pl. 7, figs. 5, 22). However, viewed from the test exterior, the pore frames are much deeper, commonly nodose, and show considerable relief (e.g., Pl. 7, figs. 19, 22). These observations suggest that test thickening occurred via the accretion of microgranular silica (probably in a lamellar mode) around pore frame rims on the exterior, but not the interior, of the test. Because all of the thoracic pore frames of a given spec- imen of Napora are of approximately the same depth, it is suggested that each time a lamella of microgranular silica was secreted, it covered the entire surface of the thorax — thus resulting in the equal development of the pore frames. This at least appears to be the case with Napora, Farcus, n. gen., and Rolumbus, n. gen. How- ever, the pore frames of Jacus De Wever, 1982, are typically inset between massive ridges and show con- siderable differences in relief. Obviously, the genetic code governing the accretion of silica on the pore frames of Jacus differed considerably from that of Napora, Farcus, and Rolumbus. Thickening of both cephalic and thoracic pore frames proceeded in the manner cited above until the proxi- mal portion of the test was covered by an outer layer of microgranular silica. On well-preserved specimens this layer is thin and commonly does not obscure pore frame rims. The thinness of this layer, as well as its superposition on cephalic and proximal thoracic pore frames, suggests that it was formed at a late stage in ontogeny. The thin, fragile nature of the tubular, ve- lum-like structure extending from the aperture (mouth) of the farcid genus Rolumbus, n. gen., and Jacus De Wever, 1982, as well as its distal position, suggests that this structure formed at a very late stage of ontogeny (Pl. 5, fig. 17). Via the model proposed above it is assumed that lamellae of microgranular silica are added to the horn(s) and feet, strengthening and lengthening these structures at the same time that pore frame thick- ening occurred. The mode of test secretion among the Hilarisiregidae differs in part from that of the Farcidae and Ultrana- poridae. The cephalic and thoracic walls of Hilarisirex Takemura and Nakaseko, 1982, consist ofa single layer of thick massive pore frames that is covered by a thin layer of microgranular silica. Pore frame rims often project through this thin layer (Pl. 8, figs. 6, 14), sug- gesting that the pore frames are high in relief on the test exterior and were formed in a fashion similar to that proposed for the Farcidae and Ultranaporidae. However, the structure of the abdomen of Hilarisirex appears to be considerably different. The abdominal walls consist of an inner latticed layer of flattened pore frames (Pl. 8, figs. 13-15, 17-19) overlain by an outer latticed layer formed by vermicular ridges. The degree of development of the outer vermicular, latticed layer is variable even with members of the same species. In some cases it can be quite dense while in others it is barely noticeable (see Pl. 8, fig. 14; Pl. 8, fig. 19). It is likely that this outer vermicular layer was secreted at a late stage in ontogeny and supplanted the normal mode of pore frame thickening and strengthening (e. g., in Rolumbus, n. gen.). Diceratigalea Takemura and Nakaseko, 1982, differs from Hilarisirex and other forms assignable to the Hilarisiregidae in the structure of its abdominal wall. Diceratigalea has not been ob- served in our North American Jurassic material. How- ever, from our analysis of the illustrations presented by Takemura and Nakaseko (1982, pl. 72, figs. 1—2; pl. 73, fig. 1), this genus appears to possess weakly- developed A-frames and pore frame structure resem- bling that of Rolumbus, n. gen., Farcus, n. gen., and Napora Pessagno, 1977a. Except for the fact that the test is tricyrtid and possesses typical hilarisiregid-type partitions at the base and top of the abdomen, this form appears more closely-related to Rolumbus (see Takemura and Nakaseko, 1982, pl. 72, figs. 2b, 2c and Hilarisirex). Suborder NASSELLARIINA Ehrenberg, 1875 Family FARCIDAE, new family Type genus. — Farcus, new genus. Diagnosis. — Test dicyrtid with single layer oflatticed meshwork on both cephalis and thorax. Latticed layer of cephalis and occasionally proximal portion of thorax covered by thin outer layer of microgranular silica. Cephalis large, hemispherical with one horn (e.g., Far- cus, n. gen.), or two horns (e.g., Rolumbus, n. gen.), which are triradiate in axial section. Cephalic skeletal elements cyrtoid, including vertical bar, primary left JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 23 lateral bar, primary right lateral bar, median bar, sec- ondary left lateral bar, secondary right lateral bar, and apical bar (dorsal bar absent). Thorax large, inflated, with four (rarely five) feet that are triradiate in axial section. Four feet opposed to two primary lateral and two secondary lateral bars; fifth foot, if present, op- posed to vertical bar. Base of thorax hemispherical with centrally-placed circular aperture (mouth) that has an imperforate rim. Thorax with (e.g., Rolumbus, n. gen.) or without (e.g., Farcus, n. gen.) fragile tubular, velum-like structure extending distally from aperture (mouth) of well-preserved specimens. Remarks.—The Farcidae, n. fam., differ from the Hilarisiregidae Takemura and Nakaseko, 1982, by having a dicyrtid rather than a tricyrtid test, by always having a single layer of latticed meshwork, and by always lacking A-frames. Furthermore, where the feet of the hilarisiregid test are continuous proximally with the A-frames, those of the farcid test commonly merge with the thoracic wall (Pl. 1, figs. 3, 11, 18; 12, 14). A single exception is one unusual specimen of Rolumbus sp. (Pl. 1, figs. 1, 16). On this specimen the two primary and secondary lateral bars unite directly with the prox- imal extensions of the feet. In this case, the innermost longitudinal ridge of a given proximal extension of a foot joins an opposing lateral bar. In spite of the differences cited above it is probable that the Farcidae gave rise to the Hilarisiregidae. The two families display the same configuration of cephalic skeletal elements (see Pl. 1, figs. 12, 14; Pl. 1, fig. 9). Noticeable in particular in both families is the absence of a dorsal bar. It is likely that Rolumbus sp. gave rise to either Hilarisirex sp. or Diceratigalea sp., through the acquisition of a tricyrtid test. In both cases this evolutionary feat was most likely accomplished through the development of A-frames on the distal nine-tenths of the thorax of Rolumbus and through the develop- ment of flattened partitions at the top and the base of A-frames (see Hilarisiregidae herein). As a result, the thorax of either Hilarisirex Takemura and Nakaseko, 1982, or Diceratigalea Takemura and Nakaseko, 1982, became reduced at the expense of the abdomen and its four characteristic A-frames. Because Diceratigalea displays similar pore frame structure to that of Ro- lumbus (see Test Construction herein) and weakly- developed A-frames, it is likely that Rolumbus gave rise to Diceratigalea and that Diceratigalea in turn gave rise to Hilarisirex. The latter evolutionary feat was most likely accomplished through the strengthening of the A-frames and the acquisition of two layers of lat- ticed meshwork (see Test Construction, pp. 21-22 and Hilarisiregidae, pp. 29-30). Range. — Lower Jurassic: upper Pliensbachian to up- per Toarcian. Occurrence. — Nicely Formation, Hyde Formation, and the Warm Springs Member of the Snowshoe For- mation, east-central Oregon. San Hipólito Formation, Baja California Sur. Tethyan Realm; ? Boreal Realm. Genus FARCUS, new genus Type species. — Farcus graylockensis, n. sp. Etymology of name.— Farcus (masc.) is a name formed by an arbitrary combination of letters (ICZN, 1964, Appendix D, pt. VI, Recommendation 4, p. 113). Diagnosis. — Test as with family but possessing a sin- gle, massive apical horn that is attached to the apical bar. Thorax lacking tubular, velum-like structure dis- tally. Remarks. — Farcus, n. gen., is compared to Rolum- bus, n. gen., under the latter genus. Range.—Lower Jurassic: upper Pliensbachian to middle Toarcian. Occurrence. —Nicely Formation, Hyde Formation, and Warm Springs Member of the Snowshoe Forma- tion, east-central Oregon. Sandstone member, San Hi- pólito Formation, Baja California Sur, Mexico. Te- thyan Realm, ?Boreal Realm. Farcus asperoensis, new species Plate 3, figures 12, 16, 17, 21; Plate 11, figure 9 Etymology. — This species is named for Pico Aspero, which is located east of its type area. Diagnosis. — Cephalis medium-sized, hemispheri- cal, with single, massive triradiate horn; cephalis com- monly covered by layer of microgranular silica. Horn triradiate in axial section with rounded, longitudinal ridges and narrow grooves. Thorax with small, poly- gonal pore frames, commonly partially covered by a thin layer of microgranular silica. Four feet, medium- sized, triradiate in axial section with narrow, rounded longitudinal ridges and broad grooves. Four feet com- monly attached to base of thorax, although on some specimens two of the feet are attached part way up the thorax. Circular mouth surrounded by imperforate rim. Remarks. — Farcus asperoensis, n. sp., differs from other species of Farcus by the nature of the distinctive imperforate rim surrounding the mouth. An unde- scribed species of Farcus (Pl. 11, fig. 14) from the Hyde Formation of east-central Oregon possesses an elon- gated thorax and massive horn similar to those of F. asperoensis, n. sp. 24 BULLETIN 326 Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum minimum length of cephalis 20 22,349) 30 (9) 18 (9) length of thorax 80 80 (9) 90 (9) 70 (9) width of thorax at top 48 50:5 (9) 64 (9) 43 (9) width of thorax at base 50 61.2 (8) 70 (8) 50 (8) length of horn 48 64.6 (9) 80 (9) 48 (9) width of horn at base 13 20.4 (9) 25 (9) 13 (9) length of foot (maximum) 32 61.3 (9) 80 (9) 32 (9) Type locality. —SH-412-14 (see Appendix). Deposition of types.—Holotype: USNM 379276; paratypes: USNM 379277 and Pessagno Collection. Range. — Lower Jurassic: upper Pliensbachian so far as known (see Text-fig. 7). Occurrence. — Sandstone member, San Hipólito For- mation, Baja California Sur. ?Boreal Realm (see Text- fig. 5). Farcus graylockensis, new species Plate 2, figures 4, 6-8, 12, 15 Etymology. — Farcus graylockensis, n. sp., is named for Graylock Butte, which is located north of its type locality. Diagnosis. —Single horn wide, massive, triradiate in axial section; horn comprised of three wide, wedge- shaped grooves alternating with three wide, rounded ridges. Thorax with massive, uniformly-sized tetra- gonal and pentagonal pore frames. Feet moderately long, triradiate in axial section; three longitudinal grooves deep, wider proximally than distally, wedging out distally; three longitudinal ridges rounded, becom- ing progressively narrower distally. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 25 25.7 (10) 30 (IO 20 TON) length of thorax 100 92:5 (10): 100 010) 75 (TO) width of thorax at top 62.5 63.7 (10) 87.5 (10) 50 (10) width of thorax at base 112.5 106,2 (10): 120% 00) 100: (10) length of horn 70 72.7 (10) 87.5 (10) 62.5 (10) width of horn at base 25 23.5 (10) 25 (10) 20 (10) length of foot (maximum) 95 دورو زا‎ (O ㆍ 128 410) 75 (10) Remarks.—This species differs from similar forms among the Hilarisiregidae Takemura and Nakaseko, 1982, by possessing a dicyrtid test, and considerably different wall structure (see Pl. 1, figs. 4, 5, 10). Type locality. —OR-536 (see Appendix). Deposition of types.—Holotype: USNM 379278; paratypes: USNM 379279 and Pessagno Collection. Range. — Lower Jurassic: upper Pliensbachian (Text- fig. 7). Occurrence.—Nicely Formation of east-central Or- egon. Tethyan Realm (Text-fig. 5). Farcus species A Plate 3, figure 4 Remarks.—Farcus sp. A differs from F. graylock- ensis, n. sp., by having a ridgelike structure around the basal part of thorax. Range and occurrence. — Lower Jurassic: upper Pliensbachian to middle Toarcian. The Nicely For- mation, east-central Oregon, loc. OR-536. Tethyan Realm. Farcus species B Plate 3, figure 13 Remarks. — Similar to F. graylockensis, n. sp., but possessing five feet. Range and occurrence. — Same as for Farcus sp. A. Farcus(?) species C Plate 5, figures 7, 10 Remarks. —The massive horn and feet and sub- spherical thorax of Farcus (?) sp. C distinguish it from Farcus asperoensis. Range and occurrence. —Sandstone member, San Hipólito Formation, loc. BPW-30; upper Pliensbachi- an. Text-figure 5.— Occurrence of Lower Jurassic Nassellariina (Ul- tranaporidae Pessagno, 1977b; Farcidae, new family; and Hilarisi- regidae Takemura and Nakaseko, 1982) in east-central Oregon, Cal- ifornia, the Queen Charlotte Islands, and Baja California Sur. X = Occurrence of taxa; QC = Queen Charlotte Islands; OR = east-central Oregon; NSF — California Coast Ranges; BPW* — Viz- caino Peninsula, Baja California Sur (Sample SH-412-14 included in BPW* category on occurrence chart). 1 = Nicely Formation; 2 = Hyde Formation; 3 = Snowshoe For- mation; 4 = Franciscan Complex; 5 = San Hipólito Formation, “sandstone member”. A = lower Toarcian; B = upper Pliensbachian; C = upper Pliens- bachian?; lower Toarcian; upper Toarcian?; D = upper Toarcian. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 25 2 FAUNAL REALMS Tethyan Pe m = E E ie 0 aal 0 Gë - 51.5 CHRONOSTRATIGRAPHIC | = | 3 Jalelelo] £ | 83 = c c ㅋㄷ D 9 © E UNITS qure 3 E upper | lower LITHOSTRATIGRAPHIC Kunga Maude 1 5 UNITS Fm. Fm. SAMPLE LOCALITIES x وه آه اه أوأه اه ]+ اه هم‎ A -fojl-Iololol«ajolololo[lolol«i-[ojo 이 이 의 이 이 이 이 이 이 이 이 이 이 2۱۱ 이 و‎ نویه Farcus asperoensis, n. sp. Farcus graylockensis, m sp Farcus sp. 4 X Rolumbus gastili, n. sp. Rolumbus halseyensis, n. sp. X Rolumbus hamiltoni, n. sp. Rolumbus mirus, n. sp. X Rolumbus venustus, n. sp. X X Rolumbus sp. X X X Jacus reiferensis, n. sp. Jacus (?) sandspitensis, n. sp. XX Jacus (?) sp. aff. J. (?) sandspitensis, n. sp. Jacus sp./Jacus (?) sp. X X Á Napora cerromesaensis, n. sp. Napora (?) graybayensis, n. sp. X X Napora insolita, n. sp. Napora mitrata, n. sp. Napora morganensis, n. sp. X Napora sp. x A Á ERE 26 BULLETIN 326 Genus ROLUMBUS, new genus Type species. — Rolumbus mirus Pessagno, Whalen, and Yeh, n. sp. Etymology.— Rolumbus (masc.) is a name formed by an arbitrary combination of letters (ICZN, 1964, Appendix D, pt. VI, Recommendation 4, p. 113). Diagnosis. — Test as with family but possessing two massive horns: a vertical horn attached to the vertical bar and an apical horn attached to the apical bar. Tu- bular, velum-like structure extending from base of tho- rax on well-preserved specimens (Pl. 1, fig. 2). Remarks. — Rolumbus, n. gen., differs from Hilari- sirex Takemura and Nakaseko, 1982, by being dicyrtid rather than tricyrtid, by having only a single layer of latticed meshwork, and by lacking A-frames. It differs from Farcus, n. gen., by having two rather than one horn and by having a tubular, velum-like structure extending from the base of the thorax (see Rolumbus Sp; PI. ig. 2) Range.—Lower Jurassic: upper Pliensbachian to middle Toarcian. Occurrence. —Nicely Formation, Hyde Formation, and Warm Springs Member of the Snowshoe Forma- tion, east-central Oregon. San Hipólito Formation, Baja California Sur. Tethyan Realm. ?Boreal Realm. Rolumbus gastili, new species Plate 4, figures 1, 5, 6, 9, 12-14 Etymology. — This species is named for R. Gordon Gastil (San Diego State University, San Diego, CA) in honor of his immense contributions to our understand- ing of the geology of Baja California. Diagnosis. — Cephalis large, dome-shaped with an ir- regular layer of microgranular silica; pore frames may be exposed at base of cephalis. Horns straight; apical horn longer than vertical horn; horns triradiate in axial section with narrow, rounded, longitudinal ridges and narrow grooves; discontinuous, narrow ridges may lie between three main ridges, extending part way up horn. Thorax with very irregularly-sized and -shaped tetra- gonal and pentagonal pore frames; pore frames ar- ranged in poorly-defined transverse rows separated by ridges. Four feet of medium length, triradiate in axial section with narrow, rounded ridges and broad grooves. Mouth circular in outline. Tubular, velum-like struc- ture may be preserved at base of thorax. Remarks. —'The moderately-developed transverse ridges of Rolumbus gastili, n. sp., distinguish it from Rolumbus halseyensis, n. sp. Measurements (in um). Numbers of specimens measured are in parentheses, X — broken. holotype mean maximum | minimum length of cephalis 30 25.3 (9) 30 (9) 20 (9) length of thorax 85 76.8 (8) 90 (8) 65 (8) width of thorax at top S5 49.8 (9) 58 (9) 40 (9) width of thorax at base 100 97.3 (9) 110 (9) 75 (9) length of apical horn 90 88.3 (9) 108 (9) 60 (9) length of vertical horn 20X 52.6 (3) 60 (3) 48 (3) distance between horn tips 150 126.6 (3) 140 (3) 120 (3) length of foot (maximum) 80 69.2 (7) 80 (7) 50 (7) Type locality. — BPW-30 (see Appendix). Deposition of types.—Holotype: USNM 379280; paratypes: USNM 379281 and Pessagno Collection. Range. — Lower Jurassic: upper Pliensbachian so far as known (Text-fig. 7). Occurrence.—Sandstone member, San Hipölito Formation, Baja California Sur. ? Boreal Realm (Text- fig. 5). Rolumbus hamiltoni, new species Plate 3, figures 5, 7, 9, 14 Etymology. — This species is named for Dr. Warren G. Hamilton (U. S. Geological Survey, Denver, CO), in honor of his many contributions to the geology of western North America. Diagnosis. — Cephalis with two massive, straight, tri- radiate horns comprised of three wide, rounded lon- gitudinal ridges alternating with three narrow deep grooves; horns widely separated; vertical horn shorter than apical horn. Thorax with large, massive tetragonal and pentagonal pore frames. Four feet triradiate in axial section, with three wide, rounded longitudinal ridges alternating with three deep longitudinal grooves. Remarks. —Rolumbus hamiltoni, n. sp., differs from Rolumbus mirus, n. sp., by having shorter, more mas- sive horns and feet with wider ridges and grooves, by having a thorax with more massive, more uniformly- shaped pore frames, and by having an apical horn that is longer than the vertical horn. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 20 FAUNAL PROVINCES Northern Tethyan bas Northern Till So. Boreal Boreal MIDDLE JURASSIC UPPER JURASSIC ‘ D CHRONOSTRATIGRAPHIC [- 1 TOR من‎ Poo [el = onian ۶ ridgian oc UNITS 5c C gia : 5 8 = lower upper upper a R upper lower à e TE 2 Sis LITHOSTRATIGRAPHIC Snowshoe Formation 1 Taman Formation 2 UNITS OR MX NSF SAMPLE LOCALITIES SEES CE ES و | | اب ]وا و|هو واه اه او ام اب | واه‎ ۱ 2 o Kl ed el ajo eO olo olo 9] E] DM] هه اب اب اب اس اه‎ Kal Kal Kal ۵۱ ESI ES] EST نم‎ ES بآ تم‎ SI EI SE Kal Kal Ko} IO ۱ ۲۵ f 따따 OF tO f OF COP co f co [ co ÛÎ co ] co | co | co 이 이 0۵] 0۵0 ۱ 0۵] 0۵ ۱ 00۵ 6 0۵ ۱0۵ ۱0۵ Ko 0 ۱ 0 Hilarisirex inflatus, n. sp. X q Hilarisirex oregonensis, n. sp. X Hilarisirex sp X Napora antelopensis, n. sp. Napora baumgartneri, n. sp. Napora bearensis, n. sp. Napora bona, n. sp. Napora boneti, n. sp. Napora browni, n. sp. Napora bukryi Pessagno Napora burckhardti, n. . | Napora cosmica, n. sp. | Napora sp. aff. N. cosmica, n. sp. Napora deweveri Baumgartner Napora sp. cf. N. deweveri Baumgartner Napora fructuosa, n. sp. Napora heimi, n. sp. x Napora sp. aff. N. heimi, n. sp. Napora horrida, n. sp. Napora izeensis, n. sp. X Napora lospensis Pessagno Napora maritima, n. sp. Napora moctezumaensis, n. sp. Napora sp. aff. N. moctezumaensis, n. sp. Napora opaca, n. sp. Napora tumultuosa, n. sp. Napora turgida, n. sp. Napora vegaensis, n. sp. Napora sp. Text-figure 6.—Occurrence of Middle and Upper Jurassic Nassellariina (Ultranaporidae Pessagno, 1977b; Hilarsiregidae Takemura and Nakaseko, 1982) in east-central Oregon, California, and east-central Mexico. X = Occurrence of taxa; OR = east-central Oregon; MX = eastern Mexico; NSF = California Coast Ranges. 1 = Lonesome Formation; 2 = Volcanogenic-pelagic strata above Coast Range ophiolite. 28 BULLETIN 326 Measurements (in um).—Numbers of specimens measured are in parentheses. Measurements (in um).—Numbers of specimens measured are in parentheses, X = broken. holotype mean maximum minimum holotype mean maximum minimum length of length of cephalis 37.9 20.7 (1) ESA) 23:7) cephalis 35 27.1 (6) 35 (6) 15 (6) length of thorax 125 DUDE, 125 O) 100 (7) length of thorax 55 59.6 (6) 80 (6) 50 (6) width of thorax width of thorax at top 50 50 (7) 50 (7) 50 (7) at top 60 49.8 (6) 55 (6) 44 (6) width of thorax width of thorax at base 1375 99.6(7) 137.5 (7) 100 (7) at base 90 75.8 (6) 90 (6) 55 (6) length of apical length of apical horn 75 „ 100 07) 75 (7) horn 82 JE) (9 100 (4) 54 (4) length of length of vertical horn 50 57:5. (5) 275 6) 50 (5) vertical horn 44 43.6 (5) 58 (5) 28 (5) distance distance between horn between horn tips 100 1225. OO) 100 (5) tips 155 131.2 (4) 152 (4) 98 (4) length of foot length of foot (maximum) 125 MEO 2 080. O) 100 (6) (maximum) SOX درد‎ 00 90 (4) 30X (4) Type locality. — OR-536 (see Appendix). Deposition of types.—Holotype: USNM 379282; paratypes: USNM 379283 and Pessagno Collection. Range. —Lower Jurassic: upper Pliensbachian (Text-fig. 7). Occurrence. —Nicely Formation, east-central Ore- gon. Tethyan Realm (Text-fig. 5). Rolumbus halseyensis, new species Plate 3, figures 1, 6, 18, 19 Etymology. — This species is named for Monte Hal- sey, which is located southeast of its type area. Diagnosis. — Cephalis large, hemispherical, with lay- er of microgranular silica and small nodes. Horns straight to slightly curved downward, apical horn much larger than vertical horn; horns triradiate in axial sec- tion with narrow, rounded, longitudinal ridges and broad grooves; small pores may be open at base of horns. Thorax with small tetragonal and pentagonal pore frames, commonly obscured by layer of micro- granular silica?; pore frames arranged in poorly-de- fined transverse rows separated by transverse ridges. Four feet of moderate length, triradiate in axial section with narrow, rounded ridges and broad grooves. Mouth circular in outline. Tubular velum-like structure com- monly extending from base of thorax. Remarks. This species is compared to Rolumbus gastili, n. sp., under the latter species. Type locality. —SH-412-14 (see Appendix). Deposition of types.—Holotype: USNM 379353; paratypes: USNM 379354 and Pessagno Collection. Range. Lower Jurassic: upper Pliensbachian so far as known (Text-fig. 7). Occurrence. —Sandstone member, San Hipólito For- mation, Baja California Sur, ? Boreal Realm (Text-fig. 5). Rolumbus mirus, new species Plate 5, figures 1, 11, 16, 17; Plate 11, figures 15, 19 Etymology. —(L.) mirus = wonderful, astonishing. Diagnosis. — Cephalis hemispherical, imperforate, with two slender, straight, triradiate horns connected to apical and vertical bars; horns comprised of three narrow ridges alternating with three narrow grooves; vertical horn slightly shorter than apical horn. Thorax lobulate with wall thicker proximally; thorax and tho- racic velum with mixture of variably-sized triangular (rare), tetragonal (rare), pentagonal and hexagonal pore frames with narrow rims. Four feet slender, triradiate with three narrow ridges alternating with three wide grooves, grooves about twice the width of ridges; feet extending out from just below the middle part of thorax and internally aligned with four cephalic skeletal ele- ments (two primary right lateral and two secondary left lateral bars). Aperture (mouth) circular in outline with imperforate rim and cylindrical velum in well- preserved specimens. Remarks. — Rolumbus mirus, n. sp., differs from R. hamiltoni, n. sp., by having slender horns and feet, by having more fragile (less massive) pore frames, and by having a more cylindrical velum. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 29 Measurements (in um).—Numbers of specimens measured are in parentheses. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum minimum holotype mean maximum minimum length of length of cephalis 25 24 (10) 37 (10) 13 (10) cephalis 25 26.2 (6) 32.5 (6) 25 (6) length of thorax 71 75 )10( 100 )10( 38 )10( length of thorax 100 72:96) 100 (6) 62.5 (6) width of thorax width of thorax at top 50 45 (10) 50 (10) 25 (10) at top 50 49.6 (6) 50 (6) 47.5 (6) width of thorax width of thorax at base 100 103 (10) 125 (10) 55 (10) at base 125 107:5:(6) 125 (6) 92.5 (6) length of foot length of foot (maximum) 170 134 (8) 170 (8) 63 (8) (maximum) 115 CV! 1005565) length of apical length of apical horn 88 70 (9) 88 (9) 50 (9) horn 62.5 10> ©) 82.5 (5) 52.515) length of length of vertical horn 100 89 (8) 100 (8) 75 (8) vertical horn 75 72.5 (6) 52.6) 52.5 (6) distance distance between horn between horn tips 175. 161 (7) 175 (7) 138 (7) tips 125 125.5 (5) 15050) 102 (5) Type locality.—OR-600 (see Appendix). Deposition of types.— Holotype: USNM 379284; paratypes: USNM 379285 and Pessagno Collection. Range.—Lower Jurassic: lower Toarcian (Text-fig. 7). Occurrence. — The Hyde Formation, east-central Or- egon. Tethyan Realm (Text-fig. 5). Rolumbus venustus, new species Plate 5, figures 2, 3, 18 Etymology. —(L.) venustus = graceful. Diagnosis.—Cephalis imperforate, hemispherical, with two straight horns; horns triradiate, moderate in length, vertical horn commonly slightly shorter than apical horn. Thorax trapezoidal in side view, com- prised of variably-sized polygonal pore frames with narrow rims and sides. Four feet moderate in length, straight, triradiate with three narrow ridges alternating with three wide grooves, one ridge of each foot ex- tending upward to top of thorax. Remarks. — Rolumbus venustus, n. sp., differs from R. mirus, n. sp., by having thorax with trapezoidal outline in side view. Type locality. — OR-600 (see Appendix). Deposition of types. — Holotype: USNM 379286; paratypes: USNM 379287 and Pessagno Collection. Range.—Lower Jurassic: upper Pliensbachian to middle Toarcian (Text-fig. 7). Occurrence. — The Nicely Formation, the Hyde For- mation, and the Warm Springs Member of the Snow- shoe Formation, east-central Oregon. Tethyan Realm (Text-fig. 5). Family HILARISIREGIDAE Takemura and Nakaseko, 1982 (corrected name) Type genus. — Hilarisirex Takemura and Nakaseko, 1982 (emended herein). Emended definition. — Test tricyrtid with four feet and one or two massive horns (PI. 1, fig. 4; Pl. 8, figs. 12, 18, 19). Feet and horns triradiate in axial section with three longitudinal ridges alternating with three longitudinal grooves. Cephalis with primary left lat- eral, primary right lateral, vertical, median, secondary left lateral, secondary right lateral, and apical bars; dorsal bar absent in cyrtoid configuration of cephalic skeletal elements. Cephalic and thoracic walls pos- sessing an inner latticed layer of polygonal pore frames and an outer layer of microgranular silica. Thorax small, trapezoidal in outline, separated from abdomen by an internal partition which is welded to top of A-frame (see below and Pl. 1, fig. 17). Abdominal wall either single-layered (Diceratigalea Takemura and Nakaseko, 1982) or double-layered (Hilarisirex Takemura and Nakaseko, 1982); when single-layered consisting of massive polygonal pore frames of high relief; when double-layered consisting of an inner layer of smooth, flattened pore frames overlain by a layer consisting of 30 BULLETIN 326 irregularly-arranged, interconnected bars forming a vermicular pattern and irregularly-shaped pore frames (Pl. 8, figs. 13, 14, 17-19). Abdomen four-sided. Each side comprised of an A-frame component formed by feet and their proximal extensions. Feet and their prox- imal extensions welded internally to corners of im- perforate square partitions that occur at the base of the thorax and abdomen. Internal partition at base of ab- domen giving rise internally to latticed partition with circular aperture (mouth); aperture bordered by raised, imperforate rim (Pl. 1, figs. 6, 17). Four feet opposed to two secondary and two primary lateral bars. Remarks.—The Hilarisiregidae differ from the UI- tranaporidae Pessagno (1977b) by possessing a tricyr- tid test with four feet, by lacking a dorsal bar (Pl. 1, fig. 17) among the cephalic skeletal elements, and by possessing A-frames (Pl. 1, figs. 4, 17; Pl. 8, figs. 17— 19). Early Jurassic forms included in this report in the Farcidae, n. fam., are most likely ancestral to the Hi- larisiregidae (see Farcidae, herein). The Hilarisiregidae are compared to the Farcidae under the latter family. Takemura and Nakaseko (1982, pp. 442-464) in- cluded the Hilarisireginae (= their Hilarisirecinae) in the Palaeoscenidiidae Riedel, 1967. Their definition (p. 457) of the Hilarisireginae is as follows: “Palaeo- scenidiidae with two apical spines and four basal spines, possessing poreless and spherical cephalis in the apical hemisphere and thorax in the basal hemisphere. Me- dian bar, two apical spines composing cephalic skeletal elements." Takemura and Nakaseko (1982, p. 458) noted that the cephalis of members of this subfamily includes seven cephalic skeletal elements that may cor- respond to those of the Nassellariina: a median bar, an apical bar, a vertical bar, two lateral bars (= primary lateral bars sensu Goll, 1968, p. 1413; Pessagno, 1969, p. 423), and two secondary lateral bars. They also noted correctly that a dorsal bar is absent. We feel that the definition presented by Takemura and Nakaseko (1982) 1s inaccurate. To begin with, the Hilarisiregidae are virtually unrelated to the Palaeo- scenidiidae Riedel, 1967. The four basal spines are in fact four feet that are not connected to the cephalic skeletal elements; the feet and their proximal exten- sions form the sides of the abdominal A-frames de- scribed above. As noted by Dumitrica (1978, p. 40) the four divergent basal spines of Palaeoscenidium De- flandre, 1953, emerge apically from the center of a very short bar. The test of Hilarisirex Takemura and Na- kaseko, 1982, is clearly tricyrtid and not dicyrtid as claimed by Takemura and Nakaseko; it includes a well- defined cephalis, a well-defined thorax, and a well- defined abdomen (Pl. 1, fig. 17). The cephalis and thorax (= cephalis of Takemura and Nakaseko, 1982) consists of a latticed, perforate inner layer, which on well-pre- served specimens is covered by an outer layer of mi- crogranular silica. It is likely that the microgranular outer layer was formed at a late stage in ontogeny; immature specimens probably possess a perforate, lat- ticed cephalis and thorax. On some specimens the rims of polygonal pore frames can be seen projecting through the thin veneer of microgranular silica (Pl. 8, figs. 6, 14). The abdominal wall of the type genus Hilarisirex possesses two latticed layers whereas that of Dicera- tigalea Takemura and Nakaseko, 1982, possesses a single latticed layer. Range. —Middle Jurassic (Aalenian?); lower Bajo- cian to Upper Jurassic (upper Kimmeridgian/lower Ti- thonian). Occurrence. — Snowshoe Formation of east-central Oregon; Eugenia Formation of Baja California Sur; volcanogenic-pelagic strata above the Coast Range ophiolite, California Coast Ranges; Mino Belt of cen- tral Japan. Tethyan Realm to Boreal Realm. Genus HILARISIREX Takemura and Nakaseko, 1982 Type species. —Hilarisirex quadrangularis Take- mura and Nakaseko, 1982. Emended definition. — Test as with family but pos- sessing a vertical horn and an apical horn connected to vertical and apical bars respectively. Abdomen with an inner latticed layer of flattened, smooth polygonal pore frames and an outer latticed layer consisting of irregular, interconnecting bars that form a vermicular pattern, and irregular polygonal pore frames. Remarks. — Hilarisirex Takemura and Nakaseko, 1982, differs from Diceratigalea Takemura and Na- kaseko, 1982, by having an abdominal wall with two latticed layers instead of a single one, and by having more strongly-developed A-frames. Range. —Lower Jurassic (middle Toarcian) to Upper Jurassic (upper Kimmeridgian/lower Tithonian). Occurrence. —Snowshoe Formation of east-central Oregon; Eugenia Formation, Baja California Sur; vol- canogenic-pelagic strata overlying Coast Range ophiolite at Point Sal, Santa Barbara County, Califor- nia; and Mino Belt of Central Japan. Tethyan Realm to Boreal Realm. Hilarisirex inflatus, new species Plate 1, figure 17; Plate 8, figures 4-6, 10, 13, 14, 17; Plate 11, figure 1 Etymology.—(L.) inflatus = inflated, swollen. Diagnosis. — Apical and vertical horns triradiate in axial section, nearly equal in length with three ridges of medium width alternating with three grooves of medium width; grooves and ridges gradually narrow- JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 31 ing distally and extending to tips of horns. Four feet widely separated, triradiate in axial section, about two times as long as horns; three medium-width ridges alternating with three medium-width grooves: both ridges and grooves gradually decrease in width distally. Abdomen with four inflated, convexly-arched walls linked to A-frames. Inner latticed layer of abdomen consisting of irregular, fairly uniformly-sized, tetrag- onal and pentagonal pore frames. Outer latticed layer weakly- to well-developed with irregular vermicular ridges. Remarks. — Hilarisirex inflatus, n. sp., is compared to H. oregonensis, n. sp., under the latter species. It differs from H. quadrangularis Takemura and Naka- seko, 1982 (p. 458) by having inflated abdominal walls, more widely-separated feet, and a shorter abdomen. Measurements (in um).—Numbers of specimens measured are in parentheses, X = broken. holotype mean maximum minimum length of cephalis and thorax 36.3 27.2 (9) 40 (9) 2000) length of abdomen 17256 7:728: 09) 100 (9) 65 (9) width of A-frame at top 42.9 51.6 (9) 60 (9) 40 (9) width of A-frame at base 125.4 124.3 (9) 180 (9) 100 (9) length of foot (maximum) X 127: 5*7) 165 (7) 85 (7) length of apical horn 89 85.4 (9) 112 (9) 60 (9) length of vertical horn 89 83 (7) 112 (7) 72.8 (7) distance between horn tips 122 162.4 (7) 240 (7) 120 (7) Type locality. —OR-501B (see Appendix). Deposition of types.—Holotype: USNM 379288; paratypes: USNM 379289 and Pessagno Collection. Range. —Middle Jurassic (upper Bathonian) so far as known (Text-fig. 7). Occurrence. —South Fork Member of the Snowshoe Formation, east-central Oregon. Boreal Realm (Text- fig. 6). Hilarisirex oregonensis, new species Plate 7, figures 17, 18; Plate 8, figures 12, 18, 19 Etymology. — Named for the state of Oregon. Diagnosis. — Vertical and apical horns triradiate in axial section; vertical horn commonly shorter than api- cal horn; both horns with three moderately-wide grooves alternating with three moderately-wide ridges; grooves gradually wedging out distally; ridges main- taining the same width and extending to tips of horns. Feet triradiate, about two times length of horns and displaying alternating ridges and grooves of moderate width. Abdomen elongate, having four planiform walls that are linked to A-frames. Inner latticed layer of abdomen consisting of fairly uniformly-sized trian- gular, tetragonal, and pentagonal pore frames; outer latticed layer consisting of irregular vermicular ridges that interconnect to form irregular pore frames. Remarks. — Hilarisirex oregonensis, n. sp., differs from H. inflatus, n. sp., by having an abdomen with four planiform sides, by having a more elongate ab- domen, and by usually having a shorter vertical horn. Measurements (in um).—Numbers of specimens measured are in parentheses, X — broken. holotype mean maximum | minimum length of cephalis and thorax 45 49 (7) 12 (0) 33.247) length of abdomen 100 88.9 (7) 13 66 (7) width of A-frame at top 62:5 57.9 (7) 72 0) 48.4 (7) width of A-frame at base 120 124.5 (7) 1725 0) 95.2 (7) length of foot (maximum) X — 200 (2) 118.8 (2) length of apical horn 87.5 80.9 (6) 96 (6) 58.8 (6) length of vertical horn ES 74.7 (5) 96 (3) 58.8 (5) distance between horn tips ۱73 161.8 )5( 184.8 )5( 117.6 )5( Type locality. — OR-501B (see Appendix). Deposition of types.—Holotype: USNM 379290; paratypes: USNM 379291 and Pessagno Collection. Range. — Middle Jurassic (upper Bathonian) so far as known (Text-fig. 7). Occurrence. —Snowshoe Formation of east-central Oregon. Boreal Realm (Text-fig. 6). Hilarisirex species A Plate 7, figures 1, 20 Range and occurrence. — Middle Jurassic (lower Ba- jocian) (loc. OR-594). Warm Springs Member of the Snowshoe Formation of east-central Oregon (see Ap- pendix). Rare. Tethyan Realm. 32 BULLETIN 326 Hilarisirex species B Plate 7, figure 16 Range and occurrence. — Middle Jurassic (lower Ba- jocian) (loc. OR-554). Warm Springs Member of the Snowshoe Formation of east-central Oregon (see Ap- pendix). Rare. Tethyan Realm. Hilarisirex species C Plate 7, figure 15 Range and occurrence. — Middle Jurassic (upper part of lower Bajocian) (loc. OR-549B). Snowshoe For- mation (undifferentiated) (see Appendix). Rare. Teth- yan Realm. Hilarisirex species D Plate 10, figure 1 Range and occurrence. — Upper Jurassic (upper Kimmeridgian: upper part of Zone 2 of Pessagno, Blome, and Longoria (1984)) (loc. NSF-907; see Ap- pendix). Volcanogenic-pelagic strata overlying Coast Range ophiolite at Point Sal, Santa Barbara County, California. Rare. Boreal Realm, Southern Boreal Prov- ince. Family ULTRANAPORIDAE Pessagno, 1977b Type genus. — Ultranapora Pessagno, 1977b (= Na- pora Pessagno, 19772). Emended diagnosis. — Dicyrtid cyrtoid Nassellariina with both cephalis and thorax comprised of a single latticed layer. Cephalis hemispherical, covered by layer of microgranular silica on well-preserved specimens; cephalis with prominent horn that may be entirely tri- radiate or partially triradiate in axial section; horn with or without subsidiary spines. Cephalis with cyrtoid ce- phalic skeletal elements including primary left lateral bar, primary right lateral bar, vertical bar, median bar, apical bar, secondary right lateral bar, secondary left lateral bar, and dorsal bar (Pl. 1, figs. 8, 15). Apical bar connected to horn; vertical bar connected to ce- phalocone or spinelike cephalocone (e.g., Jacus De Wever, 1982); cephalocone or spinelike cephalocone surrounded by circular opening in some genera (e.g., Jacus). Thorax large, hemispherical, with three prom- inent feet that are triradiate in axial section with three longitudinal ridges alternating with three longitudinal grooves. Aperture (mouth) at base of thorax with or without a thoracic velum; aperture circular to subcir- cular to subtriangular in outline, bordered by a raised imperforate rim. Remarks. — Napora differs from Jacus by lacking a thoracic velum and possessing more regular thoracic pore frames. In this report we tentatively include Jacus in the Ultranaporidae and suggest that it gave rise to Napora through the loss of the velum and the acqui- sition of more regular thoracic pore frames that are not separated by ridges. Note the unnamed dicyrtid nassellarian (ultranaporid?) (Pl. 1, fig. 7) with two feet may be a member of this family. Range. — Lower Jurassic: upper Sinemurian (?); low- er Pliensbachian to Upper Cretaceous. Occurrence. — Norld-wide in Tethyan and Boreal Realms. Genus JACUS De Wever, 1982 Type species. —Jacus coronatus De Wever, 1982. Remarks.—Jacus differs from Napora Pessagno, 1977a, 1977b, by possessing a thoracic velum. Ac- cording to De Wever (1982, pp. 204-205), Jacus differs from Napora by lacking a cephalocone. In its place there is a circular opening with a spine protruding from its center. The spine is apparently an extension of the vertical bar (cephalic skeletal element). Although De Wever infers that this spine is solid, his illustrations (pl. 12, fig. 5 = holotype) of Jacus coronatus, the type species of Jacus, clearly indicate that the spine is in fact porous. Pessagno (1977b, pl. 5, figs. 14, 21) illus- trated two types of cephalocones. One type (fig. 14) is conical and perforated by a number of slitlike pores; the other type (fig. 21) is spinelike and possesses three(?) pores. We suggest that the perforate spine figured by De Wever is representative of this latter type of ce- phalocone. Whether one calls this structure a spine or cephalocone is perhaps immaterial since it protrudes from a circular opening in the cephalic wall. No spec- imens of Napora have spines protruding from such an opening. Range.—Lower Jurassic: lower Pliensbachian (?); upper Pliensbachian; Toarcian (?). Occurrence. —Lower Jurassic: lower Pliensbachian to middle Toarcian. Tethyan Realm; ?Boreal Realm. Jacus reiferensis, new species Plate 4, figures 7, 8, 11; Plate 5, figures 6, 14 Etymology. — This species is named for Pico Reifer, which is located east of its type area. Diagnosis. — Cephalis medium-sized, hemispheri- cal, commonly covered with a thin layer of micro- granular silica; small spine may extend from base of cephalis. Apical horn massive, more than one-half length of test, distally trifurcating. Proximal two-thirds of horn triradiate in axial section with narrow, rounded ridges and broad grooves; distal portion of horn sep- arated into three tapering lobes; lobes elliptical in cross- section, approximately at right angles to long axis of test and in some specimens curving slightly downward; lobes of horn ranging from one-half to equal the length of the triradiate portion of horn. Thorax subpyramidal in outline with small- to medium-sized, slightly no- JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 33 dose, irregularly-shaped, elliptical and tetragonal pore frames; pore frames arranged in poorly-defined trans- verse rows separated by transverse ridges. Massive tri- radiate feet, attached to base of thorax, curved slightly inward. Subsidiary meshwork (velum?), with very ir- regularly-shaped and -spaced pore frames and imper- forate rim, some attached to base of thorax. Mouth subtriangular in outline. Remarks. —Jacus reiferensis, n. sp., is distinguished from Jacus coronatus De Wever, 1982, by the nature of the meshwork on the thorax and velum(?) as well as the structure of the horn. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum minimum length of cephalis 20 20.9 (11) 25 (11) 15 (11) length of thorax 50 03.1 1 ( 80 (11) 50 (11) width of thorax at top 45 43.1 (11) 50 (11) 40 (11) width of thorax at base 110 100 (11) 120 (11) 90 (11) length of horn 65 63.6 (11) 85 (11) 55 (11) width of horn at base 25 20.4 (11) 23:0) 15 (11) length of foot (maximum) 100 93.5 (10) 120 (10) 70 (10) Type locality. —BPW-30 (see Appendix). Deposition of types.—Holotype: USNM 379292; paratypes: USNM 379293 and Pessagno Collection. Range. — Lower Jurassic: upper Pliensbachian so far as known (Text-fig. 7). Occurrence. —San Hipólito Formation, sandstone member, Baja California Sur. ? Boreal Realm (Text- fig. 5). Jacus (?) sandspitensis, new species Plate 2, figures 5, 9, 13, 16, 17; Plate 11, figure 13 Etymology. — This species is named for the town of Sandspit in the Queen Charlotte Islands, British Co- lumbia. Diagnosis. —Cephalis small, hemispherical, with small cephalocone and relatively short horn. Proximal two-thirds of horn triradiate in axial section with three narrow grooves alternating with three rounded ridges of approximately the same width. Grooves often deep- ly-incised proximally, becoming shallower distally; ridges each bearing short spines before their termina- tion. Distal one-third of horn circular in axial section; lacking ridges and grooves. Thorax with very coarse, nodose polygonal pore frames; distal portion of thorax with mixture of tetragonal and pentagonal pore frames arranged in rows between angled ridges. Feet long, tri- radiate in axial section with three narrow ridges that alternate with three wide grooves; short spines occur along ridges on proximal half of each foot, suggesting velum attachment. Mouth subcircular in outline, sur- rounded by an imperforate rim. Remarks. — This species is questionably assigned to Jacus because it possesses a true cephalocone. It is conceivable that the spine extending from the “‘hole” (cephalopyle?) of De Wever's (1982) specimens of Ja- cus merely represents a remnant of a fragile cephalo- cone not preserved in his badly-etched material. The presence of a velum in J. (?) sandspitensis is probably indicated by the short spines that occur on the prox- imal half of the feet. It should be noted that some specimens of Napora, such as N. praespinifera (Pes- sagno, 1977b) and N. spinifera (Pessagno, 1977b) dis- play velum-like structure below the thorax and be- tween the proximal halves of the feet; however, we have never observed the basal closure of this velum- like structure. Jacus (?) sandspitensis differs from J. coronatus De Wever, 1982, by possessing a structurally simpler horn lacking a crownlike mass at its tip, and by having considerably longer, slender feet. Both species possess ridges at the base of the thorax, which separate rows of pore frames. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum minimum length of cephalis 25 23.8 (9) 25 (9) 15 (9) length of thorax 100 76.1 (9) 100 (9) 55 (9) width of thorax at top 50 48.0 (9) 62.5 (9) 40 (9) width of thorax at base 1.12.35 105.5 (9) 125 (9) 95 (9) length of horn 35 81.7 (7) 9257) 50 (7) width of horn at base 47.5 35.8 (9) 47.5 (9) 25 (9) length of foot (maximum) 170 147.5 (5) O O) 95 (5) Type locality. —QC-534 (see Appendix). Deposition of types.—Holotype: USNM 379294; paratypes: USNM 379295 and Pessagno Collection. Range. —Lower Jurassic: lower Pliensbachian so far as known (Text-fig. 7). Occurrence.—Lower Pliensbachian portion of the Maude Formation. Tethyan Realm (Text-fig. 5). Jacus (?) species aff. J. (?) sandspitensis, new species Plate 3, figure 2 Remarks. — This form differs from J. (?) sandspiten- sis, n. Sp., by having a much longer horn. Range and occurrence. — Lower Jurassic (upper low- er Pliensbachian to lower upper Pliensbachian) cherts 34 BULLETIN 326 from the Franciscan Complex of California (loc. NSF- 960). Tethyan Realm. Jacus (?) species A Plate 5, figure 4 Remarks. — This form is quite similar to Jacus (?) sp. aff. J. (?) sandspitensis, n. sp. It differs by having a horn with narrower ridges. Range and occurrence. —Lower Jurassic: upper Pliensbachian; ? lower Toarcian. Maude Formation, Queen Charlotte Islands, British Columbia (loc. QC- 622). Tethyan Realm. Jacus (?) species B Plate 5, figure 9 Remarks.—This form is questionably assigned to Jacus De Wever by having a spinelike cephalocone and by having ridgelike structures at the basal part of thorax that are similar to those of Jacus. Range.—Lower Jurassic: upper Pliensbachian to lower Toarcian (Text-fig. 7). Occurrence. —Nicely Formation (loc. OR-536) and the Hyde Formation (loc. OR-600), east-central Ore- gon. Tethyan Realm (Text-fig. 5). Jacus (?) species C Plate 3, figure 20 Remarks.—The absence of tapering lobes on the massive horn of Jacus (?) sp. C distinguishes it from Jacus reiferensis, n. sp. Range. —Lower Jurassic: upper Pliensbachian so far as known. Occurrence. —San Hipólito Formation, sandstone member, Baja California Sur (loc. SH-412-14). ? Boreal Realm. Genus NAPORA Pessagno, 1977a Napora Pessagno, 1977a, p. 94. Ultranapora Pessagno, 1977b, p. 38. Type species. — Napora bukryi Pessagno, 1977a. Emended diagnosis. — As with that of family but re- stricted to forms that lack a thoracic velum and may or may not have a cephalocone. Remarks. —Pessagno (1977a, 1977b) considered Napora to differ from Ultranapora by lacking a ceph- alocone. Because we have observed a cephalocone on specimens of Napora bukryi Pessagno, 1977a, the type species of Napora, this definition is no longer valid. Ultranapora must therefore be considered a junior syn- onym of Napora. Although forms that appear to lack a cephalocone may be present in our Jurassic samples, we tentatively include all such forms under Napora until the taxonomic and phylogenetic significance of the cephalocone is assessed. This more conservative approach corresponds to that of Baumgartner, De Wever, and Kocher (1980). It should be noted that ultranaporids possessing a large cephalis commonly have a large cephalocone (PI. 6, figs. 2, 16, 20; Pl. 7, figs. 10-12, 14). Generally, such forms likewise possess horns that are offset from the longitudinal axis of test growth, in a direction away from the cephalocone. Conversely, forms with a small cephalis possess a small cephalocone and a more cen- trally-placed horn. The cephalocone of N. bukryi, for example, is minute and easily overlooked. Range. — Lower Jurassic (upper Sinemurian (?); low- er Pliensbachian) to Upper Cretaceous. Occurrence. — World-wide in Tethyan and Boreal Realms. Napora antelopensis, new species Plate 8, figures 2, 3, 15, 20-23; Plate 11, figure 18 Etymology.—'This species is named for Antelope Creek, which is located near its type locality. Diagnosis. — Cephalis small, hemispherical with rel- atively short horn. Horn triradiate in axial section with three narrow ridges alternating with three narrow grooves. Three nodelike spines appearing on ridges in middle of horn; proximal one-half of each ridge about two times the width of distal half, short subsidiary grooves commonly developed on ridges on proximal one-half of horn. Thorax with mixture of variably- sized tetragonal (rare), pentagonal, and hexagonal pore frames with narrow rims and deep sides. Feet short, triradiate in axial section, somewhat incurved with three narrow grooves alternating with three narrow ridges. Aperture (mouth) subcircular in outline with imperforate rim. Remarks. — Napora antelopensis, n. sp., differs from N. lospensis Pessagno, 1977a, by having a longer, struc- turally different horn, larger and more delicate thoracic pore frames, and longer feet. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 20 24 (10) 30 (10) 20(10) length of thorax 100 82.5(10) 100 (10) 60 (10) width of thorax at top 50 65 (10) TS AGO) 50 (10) width of thorax at base 125 12212 (00008 0992/5 010) 100 (10) length of horn TS 69 (10) 80 (10) 55 (10) width of horn at base 25 25 010) 30 (10) 20 (10) length of foot (maximum) 175 112.8 (7) % (e 75 (7) JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 35 Type locality. —OR-501B (see Appendix). Deposition of types.—Holotype: USNM 379296; paratypes: USNM 379297 and Pessagno Collection. Range and occurrence. — Middle Jurassic (upper Bathonian); South Fork Member of the Snowshoe For- mation, east-central Oregon. Boreal Realm (Text-figs. 6, 7). Napora baumgartneri, new species Plate 6, figures 11, 13, 15, 19, 22-24 Etymology. — This species is named for Dr. Peter O. Baumgartner (Université de Lausanne, Switzerland), in honor of his contributions to the study of Jurassic Radiolaria. Diagnosis. —Cephalis small, hemispherical, with short horn. Horn triradiate in axial section with three medium-width grooves alternating with three rounded ridges; ridges of medium width on proximal two-thirds of horn, decreasing slightly in width distally and giving rise to weakly-developed nodelike spines on each ridge. Distal one-third of horn with shallow grooves and weakly-developed ridges. Thorax inflated, hemispher- ical with tetragonal, pentagonal, and hexagonal pore frames; pore frames somewhat nodose, varying in size, but predominantly medium-sized with wide rims. Feet triradiate in axial section, incurved with three shallow, narrow grooves alternating with three narrow ridges; ridges very high in relief, particularly on distal half of a given foot. Remarks. — Napora baumgartneri, n. sp., differs from N. cosmica, n. sp., by having a simpler, more massive horn, by having feet that are shorter and not as curved, and by having a more inflated thorax with larger pore frames. In addition the ridges on the feet of N. baum- gartneri are higher in relief distally whereas those of N. cosmica are higher in relief proximally. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum minimum length of cephalis 25 24 (10) 25 (10) 20 (10) length of thorax 8 76.2 (10) 100 (10) 50 (10) width of thorax at top TS 65 (10) 75 (10) 50 (10) width of thorax at base 100 107: (10) 125 (10) 87.5 (10) length of horn 37.5 54.2 (10) 70 (10) 37.5 (10) width of horn at base 25 23.7 (10) 25 (10) 20 (10) length of foot (maximum) 120 103.1 (10) 125 (10) 82.5 (10) Type locality. — OR-554 (see Appendix). Deposition of types.—Holotype: USNM 379298; paratypes: USNM 379299 and Pessagno Collection. Range. — Middle Jurassic: lower Bajocian (Text-fig. 3 Occurrence.— Warm Springs Member of the Snow- shoe Formation, east-central Oregon. Tethyan Realm (Text-fig. 6). Napora bearensis, new species Plate 7, figures 10-12; Plate 11, figure 7 Etymology. — This species is named for Bear Valley, which is located near its type locality. Description. — Cephalis large, hemispherical, with large cephalocone and horn of medium length. Horn triradiate in axial section with three longitudinal ridges alternating with three longitudinal grooves. Proximal two-thirds of horn two or three times the width of distal one-third and possessing medium-width parallel ridges alternating with somewhat wider grooves; ridges each giving rise to short spines at point where horn suddenly decreases in width. Distal one-third of horn with nar- rower ridges alternating with narrow, shallow, poorly- defined grooves. Thorax subpyramidal with variably- sized, predominantly large, slightly nodose pentagonal and hexagonal pore frames. Pore frames adjacent to feet and mouth commonly arranged in poorly-defined rows. Feet triradiate in axial section with three narrow, sharply-bladed ridges alternating with three wide U-shaped grooves. Feet proximally flaring slightly out- wards; distally becoming slightly incurved. Remarks. — Napora bearensis, n. sp., differs from N. browni, n. sp., by possessing more symmetrical, con- stant-sized pore frames and by having a straight, more symmetrical horn. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 25 25.2 (9) 27 (9) 25 (9) length of thorax 75 59.1 (9) 75 (9) 50 (9) width of thorax at top 50 48.6 (9) 30 (9) 37.5 (9) width of thorax at base 100 100.5 (9) 112.5 (9) 75 (9) length of horn 52/5 49.6 (8) 62.5 (8) 37.5 (8) width of horn at base 20 21:59) 22.5 (9) 17.5 (9) length of foot (maximum) 87.5 71.6 (7) 100 (7) 50 (7) Type locality. —OR-549B (see Appendix). Deposition of types.—Holotype: USNM 379300; paratypes: USNM 379301 and Pessagno Collection. Range.—Middle Jurassic: upper lower Bajocian (Text-fig. 7). Occurrence. —Snowshoe Formation (undifferentiat- ed), east-central Oregon. Tethyan Realm (Text-fig. 6). 36 BULLETIN 326 Napora bona, new species Plate 6, figures 4, 5 Etymology. —(L.) bonus = good, useful. Diagnosis. — Cephalis large, hemispherical, with well- developed large cephalocone and a medium-length horn. Horn triradiate in axial section with three me- dium-width longitudinal ridges alternating with three somewhat wider longitudinal grooves; ridges wider on proximal two-thirds of horn, flaring outwards to give rise to three short spines. Thorax pyramidal with lin- ear, circumferentially-arranged tetragonal pore frames; faces of distal one or two rows of pore frames sloping inwards. Feet incurved, triradiate in axial section with three sharply-bladed longitudinal ridges alternating with three wide longitudinal grooves; ridges high in relief. Remarks. — Napora bona appears closely related to Napora sp. A (Pl. 7, fig. 14). It differs from the latter form by possessing larger, less numerous, and more irregularly-shaped thoracic pore frames. Both forms display a row of inwardly-sloping pore frames at the base of the thorax. N. bona differs from N. cosmica, n. sp., by having a larger cephalis with a well-developed cephalocone; shorter, less curved feet; larger, less nu- merous, more irregular thoracic pore frames; a shorter, more massive horn; and an inturned row of pore frames at the base of the thorax. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 20 22:5 02) „ 17 5:07) length of thorax 37.5 32.8 (7) 37.5. ار‎ 295 0600 width of thorax at top 37,5 36.4 (7) 37.5 (7) رن لاد‎ width of thorax at base 70 TTA (GD) 95: (07) 62.5 (7) length of horn 3255 45.6 (4) 50 (4) 32.5 (4) width of horn at base 20 21.4 (7) 23.2.0 17:25:07) length of foot (maximum) 62.5 67.5 (4) 82.5 (4) 50 (4) Type locality. — OR-580 (see Appendix). Deposition of types.—Holotype: USNM 379302; paratypes: USNM 379303 and Pessagno Collection. Range. — Middle Jurassic: Aalenian to lower Bajo- cian (Text-fig. 7). Occurrence. — Warm Springs Member of the Snow- shoe Formation of east-central Oregon. Tethyan Realm (Text-fig. 6). Napora boneti, new species Plate 9, figures 3, 4, 17, 19, 23 Etymology. — This species is named for the late Dr. Federico Bonet (Institute of Petroleum, Mexico, D.F., Mexico), in honor of his many valuable contributions to Mexican micropaleontology and biostratigraphy. Diagnosis. — Cephalis small, hemispherical, with ce- phalocone and medium-length horn. Proximal one- half of horn triradiate in axial section with three deep, narrow longitudinal grooves alternating with three par- allel, massive, rounded ridges. Distal half of horn cir- cular in axial section, lacking longitudinal ridges and grooves; about one-half the width of proximal half. Thorax hemispherical with massive, nodose, relatively large pentagonal and hexagonal pore frames. Feet of medium length, triradiate in axial section with three rounded longitudinal ridges that alternate with three deep longitudinal grooves; ridges and grooves about equal in width. Remarks.— Napora boneti, n. sp., differs from N. burckhardti, n. sp., by having shorter feet and a pro- portionately smaller thorax with larger, more massive, and less numerous nodose pore frames. Furthermore, the thorax of N. boneti is hemispherical in shape, whereas that of N. burckhardti is subcylindrical. The two species share horns of similar structure and it is likely that N. boneti, n. sp., is ancestral to N. burck- hardti, n. sp. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 29 23.229) E) 17.5 (9) length of thorax 75 66.6 (9) 75 (9) 50% (9) width of thorax at top 50 53.6 (9) 62.5 (9) 37.5 (9) width of thorax at base 87.5 87.5 (9) TION) 62.5 (9) length of horn 80 63.4 (8) 80 (8) 32.5 (8) width of horn at base 228 24.4 (9) 37.5 (9) 22.5 (9) length of foot (maximum) 75 67.4 (4) 75 (4) 50 (4) Type locality. -MX-82-15 (see Appendix). Deposition of types.— Holotype: USNM 379304; paratypes: USNM 379305 and Pessagno Collection. Range. — Upper Jurassic: upper Kimmeridgian, up- per Zone 2 (Text-fig. 7). Occurrence. —Taman Formation of east-central Mexico. Tethyan Realm (Text-fig. 6). Napora browni, new species Plate 6, figures 6, 7 Etymology. — This species is named for C. E. Brown (U. S. Geological Survey), in honor of his contributions to the geology of the John Day Inlier, east-central Or- egon. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 37 Diagnosis. —Cephalis large, hemispherical, with cephalocone and wide, massive horn of medium length. Horn triradiate in axial section with three wide grooves alternating with three rounded, wide ridges. Horn asymmetrical; distal half to one-third offset from long axis of test at an angle. Grooves lenticular in outline, wide medially. Proximal half of ridges straight, devel- oping shallow subsidiary grooves that deepen towards cephalis; distal half of ridges commonly lower in relief, separated from proximal portions by sharp line of de- marcation (break in slope). Thorax hemispherical with irregularly-sized and -shaped, relatively massive te- tragonal, pentagonal, and hexagonal pore frames (pen- tagonal and hexagonal pore frames predominating). Feet short, slightly incurved, triradiate in axial section with three narrow ridges alternating with three wide grooves. Remarks. — Napora browni, n. sp., differs from all other species of Napora by virtue of the asymmetrical, crooked nature of its horn. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 20 23.7 (8) 25° (8) 20 (8) length of thorax 50 48.7 (8) 62.5 (8) 37.5 (8) width of thorax at top 50 47.5 (8) 55 ©) IWS (8) width of thorax at base 87.5 94.6 (8) 100 (8) 87.5 (8) length of horn 70 66.2 (6) 75 (0 55 (6) width of horn at : base 1255 23.7 (8) 40 (8) 12.5 (8) length of foot (maximum) 75 — 1:30 120) 78 HO) Type locality. —OR-580 (see Appendix). Deposition of types.—Holotype: USNM 379306; paratypes: USNM 379307 and Pessagno Collection. Range.—Middle Jurassic: Aalenian (?) so far as known (Text-fig. 7). Occurrence. — Warm Springs Member of the Snow- shoe Formation, east-central Oregon. Tethyan Realm (Text-fig. 6). Napora bukryi Pessagno Plate 9, figures 5, 12-14 Napora bukryi Pessagno, 1977a, pp. 94-96, pl. 12, fig. 8. Napora lospensis Pessagno, 1977a. Baumgartner, De Wever, and Kocher, 1980, p. 57, pl. 3, fig. 4. Remarks. — The holotype (Pl. 9, fig. 5) of Napora bukryi appears to have a small hemispherical thorax but actually the thorax is relatively large. The apparent small size of the thorax of the holotype was a conse- quence of the foreshortening resulting from the tilted view of the specimen. A minute cephalocone has been observed on topotypes and on specimens from locality NSF-908 (PI. 9, fig. 12). Deposition of types. — Holotype: USNM 22002. Range. — Zone 2 (upper) to Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). Upper Jurassic: upper Kimmeridgian to lower Tithonian. Occurrence. — V olcanogenic-pelagic strata above the Coast Range ophiolite at Point Sal, Santa Barbara County, California. Upper Jurassic of Greece. Boreal and Tethyan Realms. Napora burckhardti, new species Plate 10, figures 2-5, 15, 16, 21-23 Etymology. —This species is named for Carlos Burckhardt, in honor of his pioneering studies of the Jurassic stratigraphy and ammonite faunas of Mexico during the early 1900’s. Diagnosis.—Cephalis relatively large, hemispheri- cal, with medium-length horn. Proximal half of horn triradiate in axial section with three wide, rounded ridges alternating with three narrow, deep grooves; dis- tal one-half of horn circular in axial section, rapidly tapering to pointed tip. Medial portion of horn swollen due to thickening of ridges. Cephalis and proximal half of horn frequently covered with layer of microgranular silica that may obscure triradiate structure. Thorax subcylindrical in shape with medium-sized, slightly nodose tetragonal and pentagonal pore frames; pore frames arranged in poorly-defined transverse rows. Feet of moderate length, curved inwards towards long axis of test; with three wide grooves alternating with three narrow, rounded ridges. Mouth circular in outline, bounded by imperforate rim. Remarks. — Napora burckhardti, n. sp., differs from Napora lospensis Pessagno, 1977a, by having a sub- cylindrical thorax with wider, less massive pore frames, a considerably longer, less massive horn, which is cir- cular in axial section distally, and much longer, more curved feet. N. burckhardti differs from N. bukryi Pes- sagno, 1977a, by having a subcylindrical thorax, a longer horn with different structure, and longer feet. 38 BULLETIN 326 Measurements (in um).—Numbers of specimens measured are in parentheses. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum minimum holotype mean maximum minimum length of cephalis 25 25.5 (10) 30 (10) 25 (10) length of thorax o 73.7 (10) 7 (80) 62.5 (10) width of thorax at top 87.5 TOMO) 87.5 (10) 70 (10) width of thorax at base 112.5 10610), 125 000) 7 le length of horn 75 13.3 (10) 87.5 (10) 67.5 (10) width of horn at base 25 23.7 (10) 25 00 20 (10) length of foot (maximum) 1195 104.6 (10) 112.5 (10) 100 (10) length of cephalis 20 16.8 (11) 20 (11) IS (11) length of thorax 80 70.5 (10) 80 (10) 60 (10) width of thorax at top 40 38.1 (11) 45 (11) 30 (11) width of thorax at base 90 99.5 (11) 110 (11) 90 (11) length of horn 70 86.3 (11) 100 (11) 70 (11) width of horn at base 20 22 25 (11) 20 (11) length of foot (maximum) 80 95.9 (11) 120 (11) 70 (11) Type locality. — MX-81-54 (see Appendix). Deposition of types.— Holotype: USNM 379308; paratypes: USNM 379309 and Pessagno Collection. Range and occurrence. — Upper Jurassic: lower Ti- thonian portion of Taman Formation, east-central Mexico. Tethyan Realm (Text-figs. 6, 7). Napora cerromesaensis, new species Plate 4, figures 2-4, 10, 15, 16 Etymology. — This species is named for Cerro Mesa, located to the northeast of its type locality. Diagnosis. — Cephalis relatively small, hemispheri- cal, with massive apical horn; cephalis may be partially obscured by a thin layer of microgranular silica. Horn approximately same length as test, triradiate in axial section with narrow, rounded, longitudinal ridges al- ternating with broad, deep grooves; ridges extended into broad spines midway from base to terminus of horn; narrow ridges of apical horn may extend down over cephalis, although not as pronounced as on horn; horn tapers distally. Thorax subpyramidal in shape with large, irregularly-shaped tetragonal and pentag- onal pore frames arranged in poorly-defined transverse rows. Massive triradiate feet attached to base of thorax, curved slightly inward. Mouth subtriangular in outline, surrounded by imperforate rim. Remarks. — Napora cerromesaensis, n. sp., is distin- guished from Napora (?) graybayensis, n. sp., by the more regular arrangement of the pore frames and the thin layer of microgranular silica on the cephalis. In addition, N. cerromesaensis possesses a more massive horn and feet that are not as curved as those of N.(?) graybayensis, n. sp. Type locality. — BPW-30 (see Appendix). Deposition of types.—Holotype: USNM 379321; paratypes: USNM 379322 and Pessagno Collection. Range. — Lower Jurassic: upper Pliensbachian, so far as known (Text-fig. 7). Occurrence. —San Hipólito Formation, sandstone member, Baja California Sur. ?Boreal Realm. Nicely Formation, east-central Oregon. Tethyan Realm (Text- fig. 5). Napora cosmica, new species Plate 7, figures 2, 5-7, 19, 21, 22; Plate 11, figure 10 Etymology. —(L.) cosmicos — belonging to the world. Diagnosis. — Cephalis small, hemispherical, with medium-length horn. Horn basically triradiate in axial section, having three wide ridges alternating with three shallow, wide grooves. Proximal two-thirds of horn with subsidiary grooves developed on primary ridges (Pl. 7, figs. 19, 22) resulting from bifurcation of a given primary ridge. Distal one-third of horn with the de- velopment of short, nodelike spines (usually three) on primary ridges. Thorax pyramidal with variably-sized pentagonal and hexagonal pore frames and very long curved feet (Pl. 7, figs. 2, 5). Feet triradiate in axial section with three wide grooves alternating with three narrow ridges. Ridges higher in relief on proximal half of a given foot. Proximal half of each foot curving outwards away from axis of test; distal half of each foot curving towards the axis of test growth. Remarks. —'This species differs from other species of Napora by virtue of its long, peculiarly-curved feet. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 39 Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 20 20.5 (9) 25 (9) 20 (9) length of thorax 50 99:519) 65 (9) 45 (9) width of thorax at top 50 48.8 (9) 55 (9) 40 (9) width of thorax at base PEAS 105.2 (9) 120 (9) 90 (9) length of horn 50 55.5 (9) 85 (9) 40 (9) width of horn at base 2915 24.4 (9) 30 (9) 20 (9) length of foot (maximum) 125 112.7 (9) 135 (9) 85 (9) Type locality. —OR-513 (see Appendix). Deposition of types.— Holotype: USNM 379323; paratypes: USNM 379324 and Pessagno Collection. Range. —Middle Jurassic: lower upper Bajocian (Text-fig. 7). Occurrence. —South Fork Member of the Snowshoe Formation, east-central Oregon. Tethyan Realm (Text- fig. 6). Napora species aff. N. cosmica, new species Plate 6, figure 8 Remarks. — This form closely resembles N. cosmica, n. Sp., but differs by having a smaller thorax with less numerous pore frames. Range and occurrence. — Middle Jurassic (Aaleni- an?) Warm Springs Member of the Snowshoe For- mation (loc. OR-580; rare). Tethyan Realm (Text-figs. 0. i Napora deweveri Baumgartner, sensu lato Plate 10, figure 14 Napora deweveri Baumgartner, 1980b, pp. 56-57, pl. 3, figs. 1-3, 5; pl. 6, fig. 9. Remarks. —Our specimens of N. deweveri appear to possess slightly larger thoracic pores and a longer horn than displayed by Baumgartner’s types. We see no evi- dence of a cephalocone on either Baumgartner’s spec- imens or ours. Range and occurrence. — Upper Jurassic: lower Ti- thonian. Taman Formation of east-central Mexico. Tethyan Realm (Text-figs. 6, 7). Napora species aff. N. deweveri Baumgartner Plate 10, figure 19 Range and occurrence.—Upper Jurassic: lower Ti- thonian. Zone 3 (sensu Pessagno, Blome, and Longo- ria, 1984) loc. MX-82-20. Taman Formation of east- central Mexico. Tethyan Realm (Text-figs. 6, 7). Napora fructuosa, new species Plate 6, figures 1-3; Plate 11, figure 6 Etymology. —(L.) fructuosus = fertile. Diagnosis. — Cephalis low, broad, hemispherical, with short, stout horn; horn triradiate in axial section with three broad ridges alternating with three narrow grooves. Thorax broad, hemispherical, with numerous small, slightly nodose pentagonal and hexagonal pore frames. Feet very narrow, long, incurved, triradiate in axial section with three narrow longtitudinal ridges alternating with three narrow grooves. Remarks. — Napora fructuosa, n. sp., differs from N. lospensis Pessagno, 1977a, by having smaller, much less massive pore frames, a less massive horn, and longer, considerably thinner feet. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 20 23 (00) 259° (10) = 25 (10; length ofthorax 100 82.5 (10) 100 (10) 50- (10) width of thorax at top 75 70.7 (10) 72 (10) -30 O0 width of thorax at base EIS 106.5 (10) 117.5 (100 97:510) length of horn 29 22.5 (10) 257 * 00) 12:5 (19) width of horn at base 50 46.1 (10) 50 (00) 37.5410) length of foot (maximum) 100 93.3 (6) 125 (6) 62.5 (6) Type locality. — OR-593 (see Appendix). Deposition of types. —Holotype: USNM 379325; paratypes: USNM 379326 and Pessagno Collection. Range. —Lower Jurassic: Middle Jurassic: Aalenian (Text-fig. 7). Occurrence. — Narm Springs Member, Snowshoe Formation, east-central Oregon. Tethyan Realm (Text- figs. 5, 6). Napora (?) graybayensis, new species Plate 2, figures 1-3, 10, 11, 14; Plate 11, figures 3, 4 Etymology. — This species is named for Gray Bay, which is located north of its type locality. Diagnosis. — Cephalis relatively small, hemispheri- cal, with massive horn; pore frames of cephalis com- monly not covered by layer of microgranular silica. Horn triradiate in axial section throughout most of its length, with three narrow, rounded, longitudinal ridges alternating with three broad, shallow grooves; horn tapering sharply distally; length of horn one-half to equal to length of test; small spines commonly located on ridges approximately at midpoint of horn. Thorax subpyramidal in shape with medium- to very large- 40 BULLETIN 326 sized, irregularly-shaped, tetragonal to pentagonal pore frames; pore frames arranged in poorly-defined trans- verse rows with slight development oftransverse ridges separating the rows. Feet of moderate length, curved inward, triradiate in cross-section, consisting of three very narrow, longitudinal ridges alternating with broad shallow grooves. Mouth triangular in outline, bounded by narrow, imperforate rim. Remarks. — This species of Napora is distinguished from others by the irregular shape and distribution of the pore frames. It is questionably assigned to the genus Napora because of its peculiar, irregular pore frames, poor definition externally between the cephalis and thorax, and the lack of a microgranular layer proxi- mally. Measurements (in um). Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 10 13.3 (9) 20 (9) 10 (9) length of thorax 50 56.6 (9) 75 (9) 45 (9) width of thorax at top 30 36.6 (9) 45 (9) 30 (9) width of thorax at base 50 69.4 (9) 80 (9) 50 (9) length of horn 50 42.2 (7) 60 (7) 30 (7) width of horn at base 12:5 14.1 (9) 20 (9) 10 (9) length of foot (maximum) 30 65 (8) 80 (8) 45 (8) Type locality. — QC-675 (see Appendix). Deposition of types.—Holotype: USNM 39327: paratypes: USNM 379328 and Pessagno Collection. Range. — Upper Sinemurian, so far as known (Text- fig. 7). Occurrence. — Kunga Formation, black argillite member, Queen Charlotte Islands, British Columbia. Tethyan Realm (Text-fig. 5). Napora heimi, new species Plate 10, figures 8, 10-12, 17, 20, 24 Etymology. — This species is named for Arnold Heim, in honor of his pioneering investigations ofthe geology of the Sierra Madre Oriental in the early 1900's. Diagnosis. — Cephalis relatively large, hemispheri- cal, with very wide, massive horn of medium length. Horn triradiate in axial section with three eccentric grooves alternating with three eccentric ridges; grooves wide medially, lenticular in outline; ridges wide, mas- sive, gradually becoming narrower distally; ridges higher in relief and developing nodes in middle portion of horn, lending a swollen appearance to horn medially. Cephalis and proximal portion of horn may be covered by layer of microgranular silica. Thorax rounded, hemispherical, with symmetrical, medium-sized, slightly-nodose pentagonal and hexagonal pore frames. Feet triradiate in axial section and of medium length, curved slightly towards long axis of test; feet consisting of three medium-width longitudinal grooves alternat- ing with three rounded, medium-width ridges. Remarks.— Napora heimi, n. sp., appears closely re- lated to Napora deweveri Baumgartner, 1980b. It dif- fers from N. deweveri by having a horn that is longer, with wide grooves of lenticular outline; by having a rounded, hemispherical thorax; by having larger and less numerous pore frames; and by having longer, less curved feet that possess ridges which are rounded rath- er than bladelike. Measurements (in um). Numbers of specimens measured are in parentheses. holotype mean maximum minimum length of cephalis 20 25.2 (10) 27.5 (10) 25.5 (10) length of thorax 62.5 7۱۱ (0) 75 (10) 62.5 (10) width of thorax at top 75 73.7 (10) 80 (10) 62.5 (10) width of thorax at base 100 101.2(10) 112.5(10) 100 (10) length of horn "o 71.7 (10) 77.5 (10) 75 (10) width of horn at base 329 29.5 (10) 37.5 (10) 2% (10) length of foot (maximum) 75 84.6 (8) 100 (8) 72.5 (8) Type locality. —MX-81-54 (see Appendix). Deposition of types.—Holotype: USNM 379329; paratypes: USNM 379330 and Pessagno Collection. Range and occurrence. — Upper Jurassic: lower Ti- thonian part of the Taman Formation, east-central Mexico. Tethyan Realm (Text-figs. 6, 7). Napora species aff. N. heimi, new species Plate 10, figure 13 Remarks. — This form differs from Napora heimi, n. sp., by having a thorax with irregular polygonal pore frames. Range and occurrence. Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). Upper Jurassic: lower Tithonian part of the Taman Formation, east-central Mexico. Tethyan Realm (Text-figs. 6, 7). Napora horrida, new species Plate 6, figures 16, 20; Plate 11, figure 5 Etymology.—(L.) horridus = horrible, uncouth. Diagnosis. — Cephalis hemispherical, with large ce- phalocone and massive medium-length horn. Horn tri- radiate in axial section with three wide, rounded, lon- gitudinal ridges alternating with three wide, longitudinal grooves. Ridges more or less parallel on proximal half JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 41 of horn, converging on distal half, maintaining same width throughout; each ridge with short nodose spine medially. Thorax subpyramidal with large, slightly no- dose, irregularly-shaped tetragonal, pentagonal, and hexagonal pore frames. Feet wide, massive, short, straight, triradiate in axial section, projecting slightly outwards. Feet with three thin, rounded, moderately high longitudinal ridges that alternate with three lon- gitudinal grooves; grooves very wide proximally, wedging out in a distal direction; ridges decreasing slightly in width distally. Remarks.— Napora horrida, n. sp., differs from N. bearensis, n. sp., by possessing a longer, wider, struc- turally-different horn; by possessing a mixture of te- tragonal, pentagonal, and hexagonal pore frames; and by possessing shorter, wider, straighter feet. Measurements (in um).—Numbers of specimens measured are in parentheses. triradiate in axial section with three narrow ridges al- ternating with three wide grooves. Remarks.— Napora insolita, n. sp., differs from other species of Napora described in this paper by having a short horn with spikelike nodes at tip. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum holotype mean maximum minimum length of cephalis 1725 24 (8) SAS) 17.5 (8) length of thorax 62.5 70.3 (8) 100 (8) 50 (8) width of thorax at top 50 53.7 (8) 75 (8) 50 (8) width of thorax at base 100 102.1 (8) 122.5 (8) ISE) length of horn 32.5 44.6 (8) 58 (8) 32.5 )8( width of horn at base 20 23.7 (8) 27.5 (8) 20 (8) length of foot (maximum) 82.5 97.5 (5) 112.5 (5) 82.5 (5) Type locality. —OR-555 (see Appendix). Deposition of types.—Holotype: USNM 379331; paratypes: USNM 379332 and Pessagno Collection. Range. — Middle Jurassic: lower Bajocian (Text-fig. T): Occurrence. — Warm Springs Member of the Snow- shoe Formation of east-central Oregon. Tethyan Realm (Text-fig. 6). Napora insolita, new species Plate 5, figures 5, 12, 13 Etymology. - (L.) insolitus = unusual, strange. Diagnosis. — Cephalis small, hemispherical; cepha- locone moderately well-developed with slitlike pores; horn short, triradiate with three narrow ridges alter- nating with three wide grooves, each ridge terminating with short spikelike node at tip of horn. Thorax conical in outline, comprised predominantly of pentagonal and hexagonal pore frames. Three feet of medium length, length of cephalis 25 31 (8) 40 (8) 25 (8) length of thorax 65 62 (8) 75 (8) 50 (8) width of thorax at top 60 59 (8) 75 (8) 50 (8) width of thorax at base 125 115 (8) 125 (8) 100 (8) length of horn 50 47 (8) 60 (8) 35 (8) width of horn at base 30 23 (8) 30 (8) 20 (8) length of foot (maximum) 125 96 (7) 130 (7) 80 (7) Type locality. —OR-589 (see Appendix). Deposition of types.—Holotype: USNM 379333; paratypes: USNM 379334 and Pessagno Collection. Range.—Lower Jurassic: upper Pliensbachian to middle Toarcian (Text-fig. 7). Occurrence. —Nicely Formation, Hyde Formation and the Warm Springs Member of the Snowshoe For- mation, east-central Oregon. Tethyan Realm (Text-fig. 5). Napora izeensis, new species Plate 8, figures 1, 7-9, 11, 16; Plate 11, figure 8 Etymology. — This species is named for the settle- ment of Izee, which is located near its type locality. Diagnosis. — Cephalis small, hemispherical, with medium-length, delicate, sharply-pointed horn. Prox- imal two-thirds of horn triradiate in axial section; distal one-third circular in axial section. Three longitudinal grooves lenticular in outline on proximal two-thirds of horn; three ridges wider and more massive proxi- mally, flaring outwards to form three nodelike spines; beyond position of nodelike spines, ridges thinner, converging and merging on distal one-third of horn. Thorax hemispherical with mixture of weakly-nodose, medium-sized pentagonal and hexagonal pore frames. Feet long, pointed, slender, triradiate; proximal half of a given foot flaring slightly outwards, extending almost directly beneath thorax; distal half of a given foot somewhat curved inwards towards long axis of test growth. Feet with three narrow, high longitudinal ridges alternating with three wide, deep grooves; grooves about two times wider than ridges. Ridges and grooves grad- ually decreasing in width distally. 42 BULLETIN 326 Remarks. — Napora izeensis, n. sp., differs from oth- er species of Napora by virtue of the distinctive struc- ture of its horn and the long, very slender nature of its feet. Whereas the proximal two-thirds of the horn are triradiate in axial section, the distal one-third is cir- cular in axial section and lacks alternating ridges and grooves. Furthermore, the three nodelike spines pres- ent medially appear to have formed from the outward flaring of the ridges. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 25 26 (10) 30 (10) 25 (10) length of thorax 87.5 79.5(10) 100 (10) 65 (10) width of thorax at top 75 69.5 (10) 87.5 (10) 60 (10) width of thorax at base 150 192:2 107015040) 120 (10) length of horn 125 93.3 (9) 12599 (9) 75 (9) width of horn at base 25 25 (LO) 30 =(10) 20 (10) length of foot (maximum) 175 140 ($5) 15/529 (5) 100 (5) Type locality. — Holotype from loc. OR-501B; para- types from locs. OR-501A, OR-501B. Deposition of types.— Holotype: USNM 379335; paratypes: USNM 379336 and Pessagno Collection. Range and occurrence. —South Fork Member of the Snowshoe Formation, east-central Oregon. Middle Ju- rassic: upper Bathonian so far as known. Boreal Realm (Text-figs. 6, 7). Napora lospensis Pessagno Plate 9, figures 11, 16 Napora lospensis Pessagno, 1977a, p. 96, pl. 12, figs. 9-10; not Baum- gartner, De Wever and Kocher, 1980, p. 57, pl. 3, fig. 4. Remarks. — The form figured by Baumgartner, De Wever, and Kocher (1980) as Napora lospensis Pes- sagno bears no resemblance to Pessagno's figured ho- lotype. It possesses a longer, structurally different horn; longer, less massive feet; and less massive pore frames. This form should probably be assigned to Napora buk- ryi Pessagno, 1977a. Deposition of types. — Holotype: USNM 22004. Range. — Upper Zone 2 to Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). Occurrence. — Volcanogenic-pelagic strata (Boreal strata only) overlying the Coast Range ophiolite. Bo- real Realm. Napora maritima, new species Plate 7, figures 3, 4, 13, 23; Plate 11, figure 2 Etymology. —(L.) maritimus — of the sea. Diagnosis. — Cephalis large, hemispherical, with short horn. Horn triradiate in axial section with three wide, shallow, lenticular grooves alternating with three me- dium-width, rounded longitudinal ridges; ridges each with well-developed node medially. Thorax inflated, hemispherical, with medium-sized, weakly-nodose pentagonal and hexagonal pore frames comprised of relatively wide bars. Feet triradiate in axial section, quite long and relatively straight projecting outwards from base of thorax with three narrow grooves alter- nating with three rounded ridges. Ridges gradually de- creasing in width distally; grooves maintaining about same width throughout. Remarks. — Napora maritima, n. sp., differs from N. baumgartneri, n. sp., by having longer, straighter feet that are not inturned. Furthermore, whereas the feet of N. baumgartneri possess ridges that increase con- siderably in relief distally and become bladelike, those of N. maritima remain about the same height through- out and tend to be rounded. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 222 23.4 (8) 25 (8) 20 ($8) length of thorax US 65 (8) e 50 (8) width of thorax at top 50 50 (8) 62.5 (8) 42.5 (8) width of thorax at base 122.5 104 (8) 122.5 (8) 90 (8) length of horn UD 56.2 (8) 70 (8) 50 (8) width of horn at base 9/5) 24 (8) 25 (8) 20 (8) length of foot (maximum) 175 152.9 (6) 182.5 (6) 125506) Type locality. — OR-555 (see Appendix). Deposition of types. — Holotype: USNM 379337; paratypes: USNM 379338 and Pessagno Collection. Range. — Middle Jurassic: lower Bajocian (Text-fig. Wy Occurrence. — Warm Springs Member of the Snow- shoe Formation, east-central Oregon. Tethyan Realm (Text-fig. 6). Napora mitrata, new species Plate 5, figures 8, 15; Plate 11, figures 11, 12 Etymology.—(L.) mitratus = wearing the mitra, a headdress or turban. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 43 Diagnosis. — Cephalis small, imperforate, and cov- ered with a layer of microgranular silica. Well-devel- oped cephalocone on cephalis. Horn triradiate in axial section with three ridges alternating with three grooves; horn terminating with moderately long spines pointing upward. Thorax hemispherical in outline, comprised of hexagonal, pentagonal, and tetragonal pore frames with narrow rims and slightly thicker sides. Feet rel- atively long; triradiate in axial section with three ridges alternating with three grooves, grooves slightly wider than ridges. Remarks. — Napora mitrata, n. sp., differs from N. insolita, n. sp., by having much longer spines at tip of horn. Measurements (in um). Numbers of specimens measured are in parentheses. holotype mean maximum minimum length of cephalis 25 28 (8) 35 (8) 25 (8) length of thorax 63 73 (8) 75 (8) 63 (8) width of thorax at top 50 50 (8) 60 (8) 40 (8) width of thorax at base 120 114 (8) 125 (8) 100 (8) length of horn 63 62 (8) 75 (8) 50 (8) width of horn at base 25 23 (8) 25 (8) 20 (8) length of foot (maximum) 150 149 (8) 190 (8) 110 (8) Type locality. — OR-600 (see Appendix). Deposition of types.—Holotype: USNM 379339; paratypes: USNM 379340 and Pessagno Collection. Range. —Lower Jurassic: lower Toarcian (Text-fig. ۵ Occurrence. — The Hyde Formation, east-central Or- egon. Tethyan Realm (Text-fig. 6). Napora moctezumaensis, new species Plate 9, figures 8-10, 20-22 Etymology. — This species is named for the Rio Moc- tezuma, which flows through the type area of the Ta- man Formation. Diagnosis. —Cephalis small, hemispherical, with rel- atively long, distinctive horn. Proximal half of horn triradiate in axial section with three massive, parallel, rounded longitudinal ridges alternating with three lon- gitudinal grooves; ridges and grooves about equal in width. Distal half of horn circular in axial section about one-half to one-third the diameter of proximal half. Thorax hemispherical with medium-sized pentagonal and hexagonal pore frames; pentagonal pore frames predominating. Feet of medium length, very slender, triradiate in axial section with three narrow grooves alternating with three narrow ridges. Remarks.— Napora moctezumaensis, n. sp., differs from N. burckhardti, n. sp., by having a hemispherical, proportionally smaller thorax (rather than a subcylin- drical thorax) with fewer pore frames; by having slen- der, less massive feet, and a somewhat less massive but structurally similar horn. Similarities in horn struc- ture suggest that N. moctezumaensis, N. burckhardti, n. sp., and N. boneti, n. sp., may be phylogenetically related. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 25 23 (9) 23 (9) 25 (9) length of thorax 15 73 19 75 (9) 73.9) width of thorax at top 75 70.8 (9) 75 (9) 62.5 (9) width of thorax at base 100 103.3 (9) 120 (9) 97.5 (9) length of horn 87.5 width of horn at 76.9 (9) 100 (9) 2۵ (9) base 25 24.2 (9) 27.5 (9) 20 (9) length of foot (maximum) 87.5 85.4 (7) 100 (7) 75 (7) Type locality. — MX-82-8 (see Appendix). Deposition of types.—Holotype: USNM 379341; paratypes: USNM 379342 and Pessagno Collection. Range. — Zone 2 (sensu Pessagno, Blome, and Lon- goria, 1984). Upper Jurassic: uppermost lower Kim- meridgian?; lowermost upper Kimmeridgian (Text-fig. A) Occurrence. —Taman Formation of east-central Mexico. Tethyan Realm (Text-fig. 6). Napora species aff. N. moctezumaensis, new species Plate 9, figures 6, 15 Remarks. — This form appears to be closely related to Napora moctezumaensis, n. sp. It differs from the latter species by having a shorter horn and much short- er, more slender feet. Range and occurrence. — Taman Formation of east- central Mexico; uppermost lower Kimmeridgian or lower upper Kimmeridgian (loc. MX-82-8; rare). Teth- yan Realm (Text-figs. 6, 7). Napora morganensis, new species Plate 3, 480068 ره رد‎ 10. 11. 12 Etymology.—This species is named for Morgan Mountain, which is located at its type locality. Diagnosis. —Cephalis hemispherical, medium-sized with long horn that is triradiate in axial section. Horn with three medium-width longitudinal ridges alternat- ing with three medium-width grooves; grooves and ridges maintaining about the same width throughout; tip of horn rounded, somewhat blunt in appearance. Thorax hemispherical with a mixture of medium-sized, massive pentagonal and hexagonal pore frames. Feet straight, very long, triradiate in axial section with three relatively wide longitudinal ridges alternating with three narrow longitudinal grooves; grooves and ridges main- taining same width except on distal portions of feet where they tend to become progressively narrower. Remarks. —Napora morganensis, n. sp., differs from other species of Napora by having a long, straight horn with a bluntly rounded tip and very long, straight feet. Furthermore, whereas most species of Napora possess horns with short spines or nodes along their longitu- dinal ridges, N. morganensis lacks such structures. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum minimum length of cephalis 25 25. (9) 25 (9) 2509) length of thorax 62.5 65.2 (9) 70 (9) 55 (9) width of thorax at top ID 64.7 (9) 13259) 37.5 (9) width of thorax at base 100 109.7 (9) 257309) 100 (9) length of horn 75 width of horn at 87.5 (5) 100 (5) 16) base 20 24.3 (8) 25 (8) 20 (8) length of foot (maximum) 187.5 165 (8) 187.5 (8) 150 (8) Type locality. — OR-536 (see Appendix). Deposition of types.— Holotype: USNM 379343; paratypes: USNM 379344 and Pessagno Collection. Range. Lower Jurassic: upper Pliensbachian (Text- fig. 7). Occurrence. —Nicely Formation of east-central Or- egon. Tethyan Realm (Text-fig. 5). Napora opaca, new species Plate 6, figures 14, 17, 18, 21 Etymology. —(L.) opacus = shadowy, obscure. Diagnosis. — Cephalis small, hemispherical, with rel- atively short horn. Horn triradiate in axial section with three grooves alternating with three rounded ridges; ridges of medium width on proximal two-thirds of horn, decreasing slightly in width distally and giving rise to a weakly-developed nodelike spine on each ridge. Distal one-third of horn with shallow grooves and weakly-developed ridges. Thorax inflated, hemispher- ical, with mixture of medium- to small-sized pentag- onal pore frames and medium-sized hexagonal pore frames. Three feet flaring slightly outwards below tho- rax and inturned distally; feet triradiate in axial section, consisting of three medium-width, rounded ridges al- BULLETIN 326 ternating with three medium-width, relatively deep grooves; grooves and ridges about same width, grad- ually decreasing in width in a distal direction. Remarks. — Napora opaca, n. sp., is closely linked phylogenetically to N. baumgartneri, n. sp., and N. maritima, n. sp. All three species display horns with similar structure and similar thoracic segments. N. opaca differs from N. baumgartneri by having narrow- er feet that have longitudinal ridges of much lower relief and that are not so markedly curved. N. opaca differs from N. maritima by having feet that are con- siderably shorter, not so widely-spread, and more curved. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum | minimum length of cephalis 25 26.5 (8) 37.5 (8) 25 (8) length of thorax 75 80.3(8) 100 (8) 75 (8) width of thorax at top 0215 62.5 (8) 7:588) 50 (8) width of thorax at base 120 129.6 (8) 137.5 (8) 120 (8) length of horn 55 56.2 (8) 62.5 (8) 45 (8) width of horn at base 25 24 (8) 25 (8) 20 (8) length of foot (maximum) 122 118.7 (8) 150 (8) 100 (8) Type locality. — OR-594 (see Appendix). Deposition of types.— Holotype: USNM 379345; paratypes: USNM 379346 and Pessagno Collection. Range. — Middle Jurassic: lower Bajocian (Text-fig. Di Occurrence. — Warm Springs Member of the Snow- shoe Formation. Tethyan Realm (Text-fig. 6). Napora tumultuosa, new species Plate 9, figures 1, 2, 7, 18 Etymology. —(L.) tumultuosus = confused, dis- turbed. Diagnosis.—Cephalis medium-sized, hemispheri- cal, with triradiate asymmetrical horn of medium length. Proximal half to one-third of horn with three wide, massive, rounded, curved ridges that suddenly terminate in the form of short spines; ridges on prox- imal half to one-third of horn alternating with three deep grooves that are of about the same width as the ridges. Ridges on distal one-half to one-third of horn about half as wide and lower in relief than ridges on proximal half of horn; ridges separated by three nar- row, shallow grooves. Thorax hemispherical with deep JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 45 irregular tetragonal and triangular pore frames that possess narrow bars and small nodes at vertices. Feet relatively long, broad, incurved, triradiate in axial sec- tion, composed of three narrow bladelike ridges that are very high in relief; ridges alternate with three wide grooves. Remarks.— Napora tumultuosa, n. sp., differs from all other species of Napora by the peculiar structure of its horn, coupled with the irregular nature of its tho- racic pore frames and the structure of its feet. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum minimum length of cephalis 25 25.3 (8) 27.5 (8) 25 (8) length of thorax 50 54.3 (8) 62.5 (8) 50 (8) width of thorax at top 629 66.2 (8) 87.5 (8) 62.5 (8) width of thorax at base 11935 101.8 (8) 125 (8) 100 (8) length of horn 82.5 74.2 (7) 87.5 (7) 62.5 (7) width of horn at base 25 24.6 (8) 29 (8) 22.5 (8) length of foot (maximum) 112:5 109.3 (4) 125 (4 100 (4) Type locality. — Holotype from loc. OR-501B. Para- types from locs. OR-501B, OR-501A (see Appendix). Deposition of types.—Holotype: USNM 379347; paratypes: USNM 379348 and Pessagno Collection. Range and occurrence. —South Fork Member of the Snowshoe Formation. Middle Jurassic: upper Batho- nian so far as known. Boreal Realm (Text-figs. 6, 7). Napora turgida, new species Plate 6, figures 9, 10; Plate 11, figure 17 Etymology. —(L.) turgidus = swollen. Diagnosis. —Cephalis large, hemispherical, with rel- atively massive, triradiate horn of medium length; horn with three wide, deep grooves alternating with three medium-width ridges; ridges each with single, medi- ally-placed node. Thorax large, very inflated, hemi- spherical with mixture of variably-sized, non-nodose pentagonal and hexagonal pore frames. Pore frames shallow with thin bars. Feet triradiate, wide proxi- mally, incurved, of medium length with three medium- width grooves alternating with three medium-width ridges; ridges and grooves gradually decreasing in width distally. Remarks.—Napora turgida, n. sp., differs from N. antelopensis, n. sp., by having a more massive horn, wider, more incurved feet, and shallower, more sym- metrical pore frames. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum minimum length of cephalis 25 23.7 (10) 25 (10 2027010) length of thorax Ws) 73: 110) 87.5(10) "30 (10 width of thorax at top 13 60 (10) 73 ' (10) NO) width of thorax at base 125 10735:600)- 1252 110) _ 75. 6000 length of horn 50 50.7 (10) 55: (10) 0457 0010) width of horn at base 25 23.7 (10) 20 (10) ۰ 20 010) length of foot (maximum) TS 82.5 (6) 92.5 (6) 75:6) Type locality. —OR-555 (see Appendix). Deposition of types.—Holotype: USNM 379349; paratypes: USNM 379350 and Pessagno Collection. Range. — Middle Jurassic: Aalenian to lower Bajo- cian (Text-fig. 7). Occurrence. — Warm Springs Member of the Snow- shoe Formation of east-central Oregon. Tethyan Realm (Text-fig. 6). Napora vegaensis, new species Plate 9, figure 24; Plate 11, figure 16 Etymology. — This species is named for the village of La Vega, which is located near its type locality. Diagnosis. —Cephalis broad, hemispherical, with short massive horn. Horn triradiate in axial section with three deep, narrow longitudinal grooves; primary ridges developing subsidiary grooves proximally. Tho- rax hemispherical, almost subcylindrical with medi- um-sized, symmetrical pentagonal and hexagonal pore frames; base ofthorax with prominent rounded, arched imperforate ridge occurring between two given feet and merging with innermost longitudinal ridges of feet. Feet long, thick, straight, triradiate in axial section, with three massive, rounded longitudinal ridges that alter- nate with three deep longitudinal grooves. Ridges somewhat wider than grooves, both becoming gradu- ally narrower in a distal direction. Remarks. — Napora vegaensis, n. sp., differs from N. burckhardti, n. sp., by having a shorter horn that is completely triradiate in axial section, a thorax that is less elongate and less cylindrical, and feet that are much thicker, more massive, and straighter. Measurements (in um).—Numbers of specimens measured are in parentheses. holotype mean maximum minimum length of cephalis 25 25. (10) 25 (10) 20 (10) length of thorax 100 94 (10) 100 (10) 72/59 (10) width of thorax at top 75 "mio 0) 75 (0100 50 (10) width of thorax at base 100 103 22610) _117.8(010). 100) GO) length of horn 3755 42.8 (8) 50 (8) 37.5 (8) width of horn at base DIS 00 27.5 (9) 20 (9) length of foot (maximum) 100 117-5 (10) 142.5- (LO), 100 010) Type locality.—MX-82-8 (see Appendix). Deposition of types.— Holotype: USNM 379351; paratypes: USNM 379352 and Pessagno Collection. Range. — Zone 2 (sensu Pessagno, Blome, and Lon- goria, 1984). Upper Jurassic: upper lower Kimmer- idgian/upper Kimmeridgian (Text-fig. 7). Occurrence. —Taman Formation of east-central Mexico. Tethyan Realm (Text-fig. 6). Napora species A Plate 7, figure 14 Range and occurrence. — Middle Jurassic (lower Ba- jocian). Warm Springs Member of the Snowshoe For- mation of east-central Oregon (loc. OR-554; rare). Tethyan Realm. Napora species B Plate 7, figure 8 Range and occurrence. —Middle Jurassic: lower Ba- jocian. Warm Springs Member of the Snowshoe For- mation of east-central Oregon (loc. OR-516; rare). Tethyan Realm. Napora species C Plate 10, figure 6 Range and occurrence.—Upper Jurassic: Kimmer- idgian. This form has been observed in volcanogenic- pelagic strata overlying the Coast Range ophiolite at Point Sal, Santa Barbara County (loc. NSF-907: upper part of Zone 2, sensu Pessagno, Blome, and Longoria, 1984). It also occurs in sample POB 889 (of Baum- gartner [see Baumgartner, De Wever, and Kocher, 1980, p. 65]) from Greece. Its known distribution thus ap- pears to be Southern Boreal to Central Tethyan. Napora species D Plate 6, figure 12 Remarks. —This form is similar to Napora horrida, n. sp. It differs from the latter species by having small- BULLETIN 326 er, more symmetrical and constant-sized pore frames and by having feet that are shorter and structurally different. Range and occurrence.—Middle Jurassic (Aaleni- an?). Warm Springs Member of the Snowshoe For- mation, east-central Oregon (loc. OR-593). Tethyan Realm. Napora species E Plate 10, figure 18 Range and occurrence.—Zone 4 (sensu Pessagno, Blome, and Longoria, 1984). Upper Jurassic: upper Tithonian. Taman Formation of east-central Mexico (loc. MX-82-37). Tethyan Realm. Napora species F Plate 10, figure 9 Range and occurrence.—Zone 4 (sensu Pessagno, Blome, Longoria, 1984). Upper Jurassic: upper Ti- thonian. Taman Formation of east-central Mexico. Broken forms that appear correlative with this form have been observed in upper Tithonian strata in the California Coast Ranges (loc. MX-82-37). Tethyan Realm, ?Boreal Realm. Napora species G Plate 10, figure 7 Range and occurrence.—Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). Upper Jurassic: lower Tithonian (loc. MX-81-54). Tethyan Realm. Napora species H Plate 7, figure 9 Range and occurrence. —Middle Jurassic: upper Ba- jocian. Snowshoe Formation (undifferentiated) of east- central Oregon (loc. OR-550). Tethyan Realm. APPENDIX—LOCALITY DESCRIPTIONS INTRODUCTION Localities in each geographic area are listed in as- cending order chronostratigraphically or biostrati- graphically. Formational units are discussed in the text (see Tectonostratigraphy). The following letter prefixes are used: MX = east-central Mexico (San Luis Potosi). OR = Mesozoic clastic terrane, John Day Inlier, east- central Oregon. NSF, JP, SA = California Coast Ranges. BPW, SH = Vizcaino Peninsula, Baja California Sur, Mexico. QC = Queen Charlotte Islands, British Columbia, Canada. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 47 EAST-CENTRAL OREGON, JOHN DAY INLIER SUPLEE-IZEE AREA OF DICKINSON AND VIGRASS (1965), AND ADJOINING AREAS Lower Jurassic OR-536*.—Nicely Formation. Reddish-brown weathering, dark- gray, silty mudstone and shale with abundant dark-gray to black, micritic limestone nodules varying in diameter from 15 cm to 0.9 m (6 in to 3 ft). Abundant well-preserved pyritized Radiolaria ar- ranged concentrically in flattened nodules about 7.5 cm (3 in) in diameter; 13.1 to 16.4 m (40 to 50 ft) above the base of the Nicely Formation. U. S. G. S. Izee 15’ Quadrangle: T.17S., R.27E., NE Ys of sect. 14. Southeast side of Morgan Mountain; small creek west of Elkhorn Creek. Upper Pliensbachian; equivalent to margaritatus and spinatum zones (ammonite standard zones: see Imlay, 1968). OR-600.— Hyde Formation. Massive, medium-gray, volcaniclas- tic sandstone (volcanic wacke) with occasional thin interbeds of tuffaceous mudstone and siltstone. Well-preserved silicified Radi- olaria occurring in small, dark-gray, micritic limestone nodules about 7.5 cm (3 in) in diameter. 64 m (210 ft) above base of Hyde For- mation. U. S. G. S. Izee 15’ Quadrangle: T.17S., R.28E., SW W of sect. 30. State highway 63 (Izee-Paulina road) along South Fork of John Day River just west of bridge over river (turn off to Hole-in- the-Ground). Upper Pliensbachian(?); lower Toarcian; upper Toar- cian(?). OR-589.—Warm Springs Member, Snowshoe Formation. Red- dish-brown weathering, dark-gray to medium-gray, silty mudstone and shale with limestone nodules bearing well-preserved silicified Radiolaria. Float from interval 1.5 to 3.0 m (5 to 10 ft) above and down hill from the contact with the underlying sandstone of the Hyde Formation. U. S. G. S. Izee 15’ Quadrangle: T.17S., R.28E., NE % of sect. 29 near southern boundary of sect. 20. West side of Schoolhouse Gulch, north-northwest of Izee. Ammonites from 24.6 and 26.8 m (81, 88 ft) above the contact with the Hyde Formation on the east side of Schoolhouse Gulch were submitted to Dr. Paul Smith (Univ. of British Columbia) for identification. P. L. Smith (written commun., 1982) identified these ammonites as Dumortieria pusilla Jaworski, 1926, and indicated that they are correlative with the European levesquei Standard Zone (up- permost upper Toarcian). Elsewhere in the same general area, P. L. Smith (written commun., 1982; charts) recorded Grammoceras (Hyatt, 1867) s. l. from the basal part of the Warm Springs Member and Dumortieria sp. cf. pusilla Jaworski, 1926, from a horizon ap- proximately 18.2 m (60 ft) above the base of the Warm Springs Member. These fossils were collected by Smith at Caps Creek, 2.5 km (1.7 mi) to the northeast of the Schoolhouse Gulch localities. The radiolarian assemblage at loc. OR-589 contains Praecono- caryomma parvimamma Pessagno and Poisson, 1981. Samples (Pes- sagno and MacLeod, unpublished data) from 11 to 24 m (35 to 80 ft) above the contact between the Hyde Formation and the Snowshoe Formation at Schoolhouse Gulch lack P. parvimamma and contain Parvicingula Pessagno, 19778 (s. 1.) (sensu Pessagno and Whalen, 1982) and Perispyridium tamarackense Pessagno and Blome, 1982. In the Queen Charlotte Islands, Carter (written commun., 1985) finds that Parvicingula s. l. and Perispyridium Dumitrica, 1978, make their first appearance in association with ammonites assignable to either the variabilis Standard Zone (middle Toarcian) or to the thouarsense Standard Zone (upper Toarcian). * This locality was incorrectly cited as being in sec. 12 by Pessagno and Blome (1980). Middle Jurassic OR-593.—Warm Springs Member, Snowshoe Formation. Red- dish-brown weathering, dark- to medium-gray, fissile shale with common dark-gray micritic limestone nodules bearing well-pre- served silicified Radiolaria. 36.5 m (120 ft) above base of Warm Springs Member. U. S. G. S. Izee 15“ Quadrangle: T.17S., R.28E., SE 4 of sect. 29; along boundary between sects. 20 and 29 on eastern tributary of Schoolhouse Gulch (north of Izee; Text-fig. 4). This sample is tentatively assigned to the Aalenian. The radiolarian assemblage at loc. OR-593 contains a few elements such as Napora fructuosa, n. sp., that are known in underlying Toar- cian strata (e.g., loc. OR-589). In addition, the assemblage at loc. OR-593 lacks lower Bajocian elements such as Turanta barbara Pessagno and Blome, 1982, which first appear in strata that are correlative with the discites Standard Zone (see loc. OR-555). Loc. OR-593 occurs 11.9 m (39 ft) above the occurrence of upper Toarcian ammonites (see data for loc. OR-589). OR-580.— Warm Springs Member, Snowshoe Formation. Red- dish-brown weathering, dark-gray, fissile shale with dark-gray silty limestone. Position above contact with Hyde Formation difficult to determine because of possible faulting and contortion of beds at contact. U. S. G. S. Izee 15’ Quadrangle: T.17S., R.28E., SW V of sect. 30 near bridge over South Fork of John Day River; about 46 m (150 ft) east of first turn in road to Hole-in-the-Ground. This sample is tentatively assigned to the Aalenian because it lacks Turanta barbara Pessagno and Blome, 1982, and Perispyridium fa- cetum Pessagno and Blome, 1982, which are characteristic of lower Bajocian strata bearing ammonites assignable to the discites, lae- viuscula, and sauzei Standard Zones (locs. OR-555, OR-594, OR- 595; see below). On the other hand, the ultranaporid taxa present at this locality are more closely allied to those of the lower Bajocian. Significantly, Napora fructuosa, n. sp., which is present at loc. OR- 593 (Aalenian?) and at loc. OR-589 (Toarcian; see above) is missing. Pessagno and Blome (1982) erroneously stated that loc. OR-580 is situated below a horizon where Imlay (1973) recorded Tmetoceras scissum (Benecke, 1865). Unfortunately, Pessagno misread Imlay's faunal list for U. S. G. S. Mesozoic Loc. 26756 (= Loc. D113 of Dickinson and Vigrass, 1965). Imlay (1973, p. 41, table 8) actually recorded Asthenoceras delicatum Imlay, 1973, from this locality. Imlay (1973, p. 19) indicated that in Europe Asthenoceras Buckman, 1899, occurs in Aalenian strata assignable to the murchinsonae Stan- dard Zone. However, in east-central Oregon Asthenoceras occurs in lower Bajocian strata assignable to the discites, laeviuscula, and sau- zei Standard Zones (see Imlay, 1973; Smith, 1980). Loc. OR-580 lies approximately along strike with U. S. G. S. Mesozoic Loc. 26756. OR-555.— Warm Springs Member, Snowshoe Formation. Red- dish-brown weathering, dark-gray, fissile shales with dark-gray, mi- critic limestone nodules and lenticular masses of silty limestone. Limestone nodules commonly bear well-preserved silicified Radi- olaria. Sample from loc. OR-555 was collected 70 m (230 ft) above the contact with the underlying Hyde Formation. U. S. G. S. Izee 15' Quadrangle: T.17S., R.28E., SW % of sect. 1. National Forest Road 16020 near Duncan Hollow; 2.88 km (1.8 mi) west of inter- section with state highway 63 (Izee-Paulina road). P. L. Smith (1980, fig. 6; written commun., 1982; unpublished chart) recorded Sonninia (Euhoploceras) sp. from a horizon ap- proximately 73 m (240 ft) above the contact with the Hyde For- mation and 1.5 m (5 ft) above loc. OR-555. Imlay (1973; pp. 19, 63-68) indicated that Euhoploceras Buckman, 1913, occurs in Eu- rope in the discites Standard Zone (lowermost Bajocian) and in the concavum Standard Zone (uppermost Aalenian). In east-central Or- egon Euhoploceras has not been observed in Aalenian strata con- taining Tmetoceras scissum (Benecke, 1865); it appears to be re- stricted to the lowermost Bajocian. 48 BULLETIN 326 OR-594.—Warm Springs Member, Snowshoe Formation. Red- dish-brown weathering, dark- to medium-gray, fissile shale with dark- gray, micritic limestone nodules containing silicified Radiolaria; 41 m (135 ft) above the contact with the Hyde Formation; in same succession with locs. OR-593 and OR-595. U. S. G. S. Izee 15’ Quadrangle: T.17S., R.28E., SE % of sect. 20; NE % of sect. 29; along boundary between sects. 20 and 29 on eastern tributary to Schoolhouse Gulch. Ammonites collected 2 m (7 ft) below loc. OR-594 were identified by P. L. Smith (written commun., 1982) as Lissoceras hydei Imlay, 1973, Holcophylloceras sp., Pelekodites silviesensis Imlay, 1973, and Sonninia? sp. Smith reported that this assemblage is indicative of his Zone 2 (Smith, 1980, p. 1606), which he equated with the north- western European /aeviuscula Standard Zone (upper part) and the sauzei Standard Zone (all but uppermost). Definitive elements in the radiolarian faunal assemblage at this horizon include Turanta barbara Pessagno and Blome, 1982, Peri- spyridium tamarackense Pessagno and Blome, 1982, and Zartus praejonesi Pessagno and Blome, 1980; these taxa also occur at loc. OR-555 and at loc. OR-595. They do not occur at loc. OR-554, which contains ammonites that are no older than the upper half of the sauzei Standard Zone (see below). OR-595.—Warm Springs Member, Snowshoe Formation. Red- dish-brown weathering, dark-gray, fissile shale with common dark- gray, micritic limestone nodules containing well-preserved silicified Radiolaria. 44.2 m (145 ft) above the contact with the underlying Hyde Formation in same section with locs. OR-593, OR-594. U. S. G. S. Izee 15’ Quadrangle: T.17S., R.28E., SE M of sect. 20; NE % of sect. 29; along boundary between sects. 20 and 29 on eastern tributary to Schoolhouse Gulch. Definitive elements in radiolarian assemblage same as for loc. OR- 594. Lower Bajocian (see discussion of megafossil data presented under locs. OR-594, OR-554). OR-554*.— Warm Springs Member, Snowshoe Formation. Dark- gray shale with dark-gray, micritic limestone nodules; nodules with well-preserved, silicified Radiolaria. Approximately 168 m (550 ft) above base of Warm Springs Member; east of fault of unknown displacement. U. S. G. S. Izee 15’ Quadrangle: T.17S., R.28E., SE Ya of sect. 1. National Forest Service Road 16020; 0.79 km (1.3 mi) west of intersection with state highway 63 (Izee-Paulina road). Di- vide between Duncan Hollow and Bunton Creek. Imlay (1973, p. 41; U. S. G. S. Mesozoic Loc. 28028) recorded Stephanoceras (Skirroceras) juhlei Imlay, 1964b, from this horizon. In the Izee area, Imlay indicated that this species does not range below the upper part ofthe Warm Springs Member (7 lower member of Dickinson and Vigrass, 1965) or above the lower part of the Schoolhouse Member (= middle member of Dickinson and Vigrass, 1965). He indicated (p. 19) that in Europe Skirroceras Mascke, 1907, does not range below the base of the sauzei Standard Zone or above the top of the humphriesianum Standard Zone. The radiolarian assemblage at loc. OR-554 is characterized by the presence of Zartus jonesi Pessagno and Blome, 1980, Z. jurassicus Pessagno and Blome, 1980, Turanta barbara Pessagno and Blome, 1982, Perispyridium foremanae Pessagno and Blome, 1982, P. fa- cetum Pessagno and Blome, 1982, and Parvicingula matura Pessa- gno and Whalen, 1982. This horizon occurs above the last appear- ance of Perispyridium tamarackense Pessagno and Blome, 1980, and below the first occurrence of Zartus imlayi Pessagno and Blome, 1980. * Subsequent investigations by Pessagno and MacLeod have led to a revised description of loc. OR-554; hence, data presented by Pessagno and Blome (1980), Pessagno and Whalen (1982), and Pes- sagno and Blome (1982) should be regarded as obsolete. OR-516.— Warm Springs Member, Snowshoe Formation (— lower member of Dickinson and Vigrass, 1965). Dark-gray mudstone with common dark-gray, micritic limestone nodules. U. S. G. S. Logdell 15' Quadrangle: T.16S., R.29E., SE % of sect. 21. Northwest side of state highway 63 (Izee-Paulina road) at elevation of 1585 m (5200 ft); north of Little Snowshoe Creek. 6.2 km (4.2 mi) west of Bear Valley Ranger Station. This locality corresponds to U. S. G. S. Mesozoic Locality 26773 of Imlay (1973, p. 49) who recorded the following taxa: Holcophyl- loceras sp., Dorsetensia sp., Pelekodites silviesensis Imlay, 1973, and Lamellaptychus sp. Dorsetensia Buckman, 1892, ranges from the uppermost part of the sauzei Standard Zone to the lower part of the overlying humphriesianum Standard Zone in Europe and in their South American equivalents (Smith, 1980, p. 1606; Westermann and Riccardi, 1979, p. 113). Diagnostic elements in the radiolarian assemblage include Tu- ranta barbara Pessagno and Blome, 1982, Perispyridium gemmatum Pessagno and Blome, 1982, Parvicingula matura Pessagno and Wha- len, 1982, Zartus jurassicus Pessagno and Blome, 1980, Z. imlayi Pessagno and Blome, 1980, and Z. thayeri Pessagno and Blome, 1980. OR-513.—South Fork Member, Snowshoe Formation near un- conformable contact with the overlying Trowbridge Formation. Dark- gray mudstone and graywacke; mudstone with common limestone nodules predominant. Nodules containing well-preserved silicified Radiolaria. U S. G. S. Izee 15' Quadrangle: T.17S., R.29E., SW ۸ of sect. 7. West side of state highway 63 (Izee-Paulina road) just south of junction of Johnnie Creek with Lewis (Bunton Creek-Dun- can Hollow area; same succession as at locs. OR-555 and OR-554). This horizon lies well above the first occurrence of Leptosphinctes Buckman, 1920, in the lowermost part of the South Fork Member (Imlay, 1973, p. 25; Smith, 1980, p. 1607). Furthermore, it occurs considerably above the first occurrence of Lupherites Imlay, 1973, which Smith (1980, p. 1607) recorded from the Bunton Creek-Dun- can Hollow area, in the lower part of the Schoolhouse Member. Smith (1980) and Westermann and Riccardi (1979, table 2) indicate that Lupherites and Leptosphinctes first appear at the base of the upper Bajocian (— rotundum Zone, Western Hemisphere; — subfur- catum Standard Zone and part of overlying garantiana Standard Zone, Europe). The radiolarian assemblage at loc. OR-513 differs from that at locs. OR-549A, OR-549B, OR-549C, and OR-550 (upper Bajocian, Seneca area) by possessing Turanta officerensis Pessagno and Blome, 1982, Zartus imlayi Pessagno and Blome, 1980, Pantanellium bai- leyi Pessagno and Blome, 1980, P. malheurense Pessagno and Blome, 1980, and other elements. The assemblage at loc. OR-513 thus ap- pears to represent a lower horizon in the upper Bajocian. OR-549A, OR-549B, OR-549C.—Snowshoe Formation (undif- ferentiated). Predominantly dark-gray mudstone with dark-gray mi- critic limestone nodules; mudstone with minor, thin-bedded gray- wacke. U. S. G. S. Seneca 15’ Quadrangle: T.17S., R.31E., SW % of sect. 2; prominent exposure on northeast side of U. S. Highway 395; 1.44 km (0.9 mi) south of Seneca and intersection with Shirttail Creek road; north side of Soda Valley. Locs. OR-549A and OR- 549B from mudstones in upper 6.0 m (20 ft) of 76.2 m (250 ft) succession just below massive sandstone on north end of exposure [= U. S. G. S. Mesozoic Localities 29790 and 29792; = Lupher's (1941) loc. 28; see Imlay, 1973]. Loc. OR-549C is situated approx- imately 21 m (70 ft) below locs. OR-549A and OR-549B. The pres- ence of Leptosphinctes Buckman, 1920, and Megasphaeroceras ro- tundum Imlay, 1962b, in the ammonite assemblage at Lupher Locality 28 definitely indicates that this succession is assignable to the upper Bajocian rotundum Zone or to its European equivalents (see Wes- termann and Riccardi, 1979). The radiolarian assemblage at locs. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 49 OR-549A, OR-549B, and OR-549C differs from that at upper Ba- jocian locality OR-513 by containing Parvicingula burnsensis Pes- sagno and Whalen, 1982, P. media Pessagno and Whalen, 1982, P. grantensis Pessagno and Whalen, 1982, Turanta nodosa Pessagno and Blome, 1982, T. silviesensis Pessagno and Blome, 1982, and species of Pachyonchus Pessagno and Blome, 1980 (see loc. OR-513 above). There is little question that this represents a younger assem- blage that is more closely allied to that at loc. OR-550C (see below). OR-550C.—Snowshoe Formation (undifferentiated). Predomi- nantly dark-gray mudstone and tuffaceous limestone. Sample from limestone. U. S. G. S. Seneca 15’ Quadrangle: T.17S., R.31E., NE Ya of sect. 3. Large quarried area on both sides of Shirttail Creek and Shirttail Creek Road. Sample C collected west of creek. Imlay (1973, p. 29) recorded a rich ammonite assemblage at this horizon. He indicated that these strata are definitely of late Bajocian age as shown by the presence of Spiroceras bifurcatum (Quenstedt, 1858). This taxon is characteristic of the lower and middle parts of the upper Bajocian (subfurcatum to garantiana Standard Zones in Europe and Africa; rotundum Zone, Western Hemisphere). The radiolarian assemblage at loc. OR-550C is characterized by the presence of Parvicingula burnsensis Pessagno and Whalen, 1982, P. grantensis Pessagno and Whalen, 1982, Perispyridium dumitricai Pessagno and Blome, 1982, P. packardi Pessagno and Blome, 1982, and Pachyonchus crassus Pessagno and Blome, 1980. All but the last two taxa also occur lower in the section at locs. OR-549A, OR-549B, and OR-549C. P. packardi is also known from the upper Bathonian part of the Snowshoe Formation (locs. OR-501B, OR-501C) and from the middle Callovian part of the Lonesome Formation (loc. OR-530). OR-501A, OR-501B, OR-501C.— Uppermost part of South Fork Member, Snowshoe Formation. Dark-gray mudstone with common dark-gray, micritic limestone nodules bearing well-preserved, silic- ified Radiolaria. Samples from separate limestone nodules imme- diately below the conformable contact with the overlying Trowbridge Formation. U. S. G. S. Izee 15’ Quadrangle: T.17S., R.28E., SE Ys of sect. 29. Outcrop on north side of state highway 63 (Izee-Paulina road) about 0.65 km (0.4 mi) east of settlement of Izee. Imlay (1973, pp. D7-D9, locs. 4-7) recovered an ammonite fauna from the upper part of the South Fork Member. He indicated that the ammonites are late Bathonian(?) to early Callovian in age. More recently Imlay (1981, pp. 7-10) assigned the ammonite assemblage from the upper 213 m (700 ft) of the South Fork Member near Izee to the upper Bathonian. For example, at U. S. G. S. Mesozoic Lo- cality 26778, situated about 46 m (150 ft) below the conformable contact with the overlying Trowbridge Formation, Imlay (1973, p. 7) reported Xenocephalites Spath, 1928, Bullatimorphites Buckman, 1921, Kepplerites Neumayr and Uhlig, 1892, Torricelliceras Buck- man, 1922, Iniskinites Imlay, 1975, Parareineckeia Imlay, 1962b, Cobbanites Imlay, 1962a, and Choffatia Siemiradzki, 1898. The radiolarian assemblage from locs. OR-501A, OR-501B, and OR-501C is characterized by the first occurrences of Parvicingula blackhornensis Pessagno and Whalen, 1982, P. elegans Pessagno and Whalen, 1982, P. schoolhousensis Pessagno and Whalen, 1982, P. vera Pessagno and Whalen, 1982, Ristola (?) turpicula Pessagno and Whalen, 1982, Perispyridium nitidum Pessagno and Blome, 1982, Turanta capsensis Pessagno and Blome, 1982, and numerous other taxa. Absent are species such as Perispyridium dumitricai Pessagno and Blome, 1982, Parvicingula burnsensis Pessagno and Whalen, 1982, and P. grantensis Pessagno and Whalen, 1982, which are characteristic of the upper Bajocian at loc. OR-550. OR-530.—Lonesome Formation. Interbedded graywacke and dark- gray, siliceous mudstone bearing small limestone nodules. U. S. G. S. Izee 15’ Quadrangle: T.18S., R.28E., NW % of sect. 3; about 0.16 km (0.1 mi) west of BM 4186 on road between Izee and Burns. North side of road adjacent to South Fork of John Day River on prominent meander bend. Imlay (1981, p. 11) assigned the Lonesome For- mation to the upper lower Callovian to Middle Callovian on the basis of the ammonite faunas. CALIFORNIA COAST RANGES Lower Jurassic NSF-958, NSF-959, NSF-960.—From block in melange, Fran- ciscan Complex. Red manganiferous radiolarian ribbon chert over- lying pillowed greenstone with minor recrystallized limestone. Con- tact between basalt and overlying chert seemingly conformable. U. S. G. S. Figueroa Mountain 7.5’ Quadrangle: T.7N., R.29W., sect. 9; 2.1 km (1.32 mi) west of Cachuma Camp (sect. 11), adjacent to Happy Canyon Road. Locs. NSF-958, NSF-959, and NSF-960 are situated 9 m (29 ft), 10 m (34 ft), and 11 m (37 ft) above the contact with pillowed greenstone. Diagnostic elements in the radiolarian assemblage in these samples include Canoptum anulatum Pessagno and Poisson, 1981, C. ru- gosum Pessagno and Poisson, 1981, and Canutus izeensis Pessagno and Whalen, 1982. Missing are Trillus elkhornensis Pessagno and Blome, 1980, and Gorgansium morganense Pessagno and Blome, 1980, which are present in the upper Pliensbachian strata of the Nicely Formation (east-central Oregon) and the Maude Formation (Queen Charlotte Islands, British Columbia). Missing also is Zartus Jurassicus Pessagno and Blome, 1980, which is known from Toarcian strata (Warm Springs Member, Snowshoe Formation) in east-central Oregon and from probable lower Toarcian strata (Maude Formation) in the Queen Charlotte Islands. The absence of T. elkhornensis and G. morganense in this assem- blage may indicate that these Franciscan cherts are correlative with either the lowermost part of the margaritatus Standard Zone (low- ermost upper Pliensbachian) or within the underlying davoei Stan- dard Zone (uppermost lower Pliensbachian). In Turkey, Pessagno and Poisson (1981) recorded Canoptum anulatum Pessagno and Poisson, 1981, C. rugosum Pessagno and Poisson, 1981, and Prae- conocaryomma parvimamma Pessagno and Poisson, 1981, from the lower member of the Sögütlü dere Formation. Although no mega- fossils are known from the lower member, the lowermost strata of the upper member include ammonites assignable to the margaritatus Standard Zone (lowermost upper Pliensbachian). In the Queen Char- lotte Islands, we have not observed these taxa in lower Pliensbachian radiolarian faunas associated with ammonites assignable to the ibex Standard Zone. Upper Jurassic NSF-906, NSF-907, NSF-908, NSF-909.— Volcanogenic-pelagic strata overlying the Coast Range ophiolite at Point Sal, Santa Barbara County, California. Green to black, thin-bedded tuffaceous chert with nodules and lenses of light-gray, micritic limestone. U. S. G. S. Point Sal 7.5’ Quadrangle: T.10N., R.36W., near western margin of sect. 34. NSF-906.— Green tuffaceous, radiolarian chert. 10.6 m (35 ft) above contact with ophiolite. Lower Zone 2 (sensu Pessagno, Blome, and Longoria, 1984); below first occurrence of Parvicingula Pes- sagno s. s.; upper Kimmeridgian (sensu gallico). NSF-907.—Lens of light-gray, micritic, tuffaceous limestone about 0.45 m (1.5 ft) thick. 11.5 m (38 ft) above contact with ophiolite. Upper Zone 2; above first occurrence of Parvicingula Pessagno s. s.; upper Kimmeridgian (sensu gallico). NSF-908.— Small, light-gray, micritic limestone nodules. 13.4 m (44 ft) above contact with ophiolite. Lower Zone 3 (sensu Pes- sagno, Blome, and Longoria, 1984); lower Tithonian (sensu gal- lico). 50 BULLETIN 326 NSF-909. Small, greenish-gray, micritic limestone nodule. 15.8 m (52 ft) above contact with ophiolite. SA-108, SA-109, SA-111*.—Unnamed lithostratigraphic unit above Coast Range ophiolite and below Great Valley sequence sensu stricto. Light- to medium-gray mudstone resting unconformably above the ophiolite breccia at the top of the ophiolite and conformably below the Great Valley sequence. Blocks of ophiolite breccia derived from the underlying ophiolite are included in the mudstone. In ad- dition, Hopson, Mattinson, and Pessagno (1981) indicated that sev- eral beds of dark ophiolitic microbreccia are interbedded with the mudstone. Red radiolarian cherts occurring below the ophiolite brec- cia unit contain a radiolarian assemblage with “Eucyrtidium” ptyc- tum Riedel and Sanfilippo, 1974, Acanthocircus variabilis (Squina- bol, 1914), and Ristola sp. aff. R. decora Pessagno and Whalen, 1982. This assemblage is assignable to the upper part of Zone 1 (sensu Pessagno, Blome, and Longoria, 1984) and is either late Cal- lovian or early Oxfordian in age. U. S. G. S. Paskenta 7.5’ Quad- rangle: T.23N., R.7W.; sect. 2; near Crowfoot Point. SA-108.—Laminated, medium-gray mudstone with abundant Radiolaria. 63.7 m (209 ft) above contact with ophiolite breccia. Upper Zone 2; upper Kimmeridgian (sensu gallico). SA-109.—Laminated, medium-gray mudstone with abundant Radiolaria. 60 m (197 ft) above contact with ophiolite breccia unit. Upper Zone 2; upper Kimmeridgian (sensu gallico). SA-111.—Laminated, medium-gray mudstone with abundant Radiolaria. 44.5 m (146 ft) above contact with ophiolite breccia unit. Upper Zone 2; upper Kimmeridgian (sensu gallico). JP-1.—Same unit as SA-108-111 (see above). Light-gray mud- stone with abundant Radiolaria. U. S. G. S. Paskenta 7.5’ Quad- rangle: T.23N., R.7W., sect. 2 near Crowfoot Point. Upper Zone 2; upper Kimmeridgian (sensu gallico). Sample collected by Dr. D. L. Jones (U. S. Geol. Survey, Menlo Park, CA). Jones (1975, p. 330) found Buchia rugosa (Fischer, 1830-1837) and specimens transi- tional between B. rugosa and B. concentrica (Sowerby, 1827) in samples from this horizon. The horizon of concurrence between B. concentrica and B. rugosa is correlative with the eudoxus Standard Zone and the underlying mutabilis Standard Zone (upper Kimmer- idgian, northwestern Europe) and with the eudoxus and acanthicum Standard Zones (upper Kimmeridgian, European Tethys) (see dis- cussion in Pessagno, Blome, and Longoria, 1984). QUEEN CHARLOTTE ISLANDS, BRITISH COLUMBIA Lower Jurassic QC-675.— Black argillite member, Kunga Formation. 374.3 m (1227.8 ft) above contact with middle black limestone member. Type locality of Kunga Formation; north shore of Kunga Island. Thin- bedded, dark-gray argillite with dark-gray, micritic limestone nod- ules containing well-preserved, silicified Radiolaria. Ammonites from below this horizon are assignable to the raricostatum Standard Zone of the uppermost Sinemurian. QC-590A. — Black argillite member, Kunga Formation. Type lo- cality of Kunga Formation; north shore of Kunga Island. Thin- bedded, dark-gray argillite with dark-gray, micritic limestone nod- ules containing well-preserved, silicified Radiolaria. 386.4 m (1267.5 ft) above contact with middle black limestone member. Upper Si- nemurian; raricostatum Standard Zone. * The strata at this locality are steeply overturned. QC-676.— Black argillite member, Kunga Formation. Type lo- cality of Kunga Formation; north shore of Kunga Island. Thin- bedded, dark-gray argillite with dark-gray, micritic limestone nod- ules containing well-preserved, silicified Radiolaria. 407.9 m (1337.8 ft) above contact with middle black limestone member. Upper Si- nemurian; raricostatum Standard Zone. QC-532.— Maude Formation. Type locality of Maude Formation at Maude Island. Dark-gray siliceous mudstone, siltstone, lithic sandstone, and micritic limestone. Sample from loc. QC-532 from dark-gray, micritic limestone 21 to 26 cm (8 to 10 in) thick; abun- dant, well-preserved, silicified Radiolaria. 79.4 m (269.5 ft) above base of Maude Formation. The radiolarian assemblage at this locality differs somewhat from that at locs. QC-534 and QC-537. However, its early Pliensbachian age can be established by its relation to underlying and overlying strata that contain early Pliensbachian ammonites (see Sutherland Brown, 1968, pp. 436-456 and data from localities QC-535 and QC- 537 herein). Lower Pliensbachian; ibex Standard Zone. QC-534.— Maude Formation. Type locality at Maude Island. Dark- gray, micritic limestone bed 26 cm (10 in) thick with abundant, well- preserved, silicified Radiolaria. 83.6 m (274.5 ft) above base of Maude Formation. The proximity of this locality to loc. QC-535 (see below) and the close similarity of the radiolarian assemblage to that at loc. QC-537 suggest that loc. QC-534 is of early Pliensbachian age. QC-535.— Maude Formation. Type locality at Maude Island. Len- ticular mass of dark-gray, silty, micritic limestone. 86.1 m (282.5 ft) above base of Maude Formation. An ammonite collected from this locality was identified by Dr. Ralph W. Imlay (U. S. Geological Survey, Washington, DC; report on referred fossils, Sept. 1977) as Tropidoceras actaeon (d’Orbigny, 1844). Frebold (1970, p. 445) indicated that this taxon is one of the “guide fossils” for the ibex Standard Zone (lower Pliensbachian). QC-537.—Maude Formation. Type locality at Maude Island. 15 cm (6 in) bed of medium-gray, micritic limestone with abundant, well-preserved, silicified Radiolaria. 90.7 m (297.5 ft) above base of Maude Formation; 0.9 m (3 ft) below a horizon with coarse tuffa- ceous sandstone. Three ammonites from this locality were submitted to Dr. Ralph W. Imlay (U. S. Geological Survey, Washington, DC). Imlay (report on referred fossils, Sept. 1977) identified these as Uptonia sp. and Uptonia sp. cf. U. dayiceroides Mouterde, 1951. In the Queen Char- lotte Islands U. sp. cf. U. dayiceroides Mouterde appears to be re- stricted to the ibex Standard Zone (Frebold, 1970, p. 445). QC-622.—Maude Formation. South shore of Skitegate Inlet op- posite Maude Island. Light-gray, micritic limestone with abundant, well-preserved, silicified Radiolaria. 38.2 m (125.5 ft) above the base of the Maude. This horizon lies 12.3 m (40.5 ft) above the occurrence of lower Pliensbachian ammonites assignable to the ibex Standard Zone and 44 m (144.5 ft) below the occurrence of lower Toarcian ammonites assignable to the falcifer Standard Zone (see Pessagno and Whalen, 1982, p. 162). The radiolarian assemblage present at this horizon appears to be indicative of the upper Pliensbachian. Significantly, it possesses Gor- gansium morganense Pessagno and Blome, 1980, and Trillus elk- hornensis Pessagno and Blome, 1980, which both make their first appearance in the upper Pliensbachian Nicely Formation of east- central Oregon (loc. OR-536). It lacks Zartus jurassicus Pessagno and Blome, 1980, which is present in the Maude Formation (south shore of Skidegate Inlet) at loc. QC-624, 27.4 m (90 ft) below the occurrence of lower Toarcian ammonites assignable to the falcifer Standard Zone (see Pessagno and Whalen, 1982, p. 162). In east- central Oregon Zartus jurassicus is present in upper Toarcian strata at loc. OR-589 and is profusely abundant in Aalenian(?) and lower Bajocian strata. JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 51 VIZCAINO PENINSULA, BAJA CALIFORNIA SUR Lower Jurassic SH-412-14.—Sandstone member (lower third) of San Hipólito Formation. Thin- to medium-bedded, poorly-sorted, olive-gray to light-greenish-brown, tuffaceous sandstone interbedded with silty and cherty tuffs and silty, tuffaceous, light-gray limestone. Sample from light-gray, micritic limestone nodule containing well-preserved Radiolaria. Approximately 250 m (820 ft) above the base of the sandstone member. Punta San Hipólito; type locality of the San Hipólito Formation. Upper Pliensbachian; ?Toarcian. Sample from Dr. David Barnes (SOHIO, Dallas, TX). BPW-14.— Sandstone member (lower third) of San Hipólito For- mation. Lithology same as for SH-412-14 (above). Sample from light-gray, micritic limestone nodule with well-preserved, silicified Radiolaria. 261.2 m (856.7 ft) above the base of the sandstone mem- ber. Punta San Hipólito; type locality of San Hipólito Formation. Upper Pliensbachian; ?Toarcian. BPW-28.— Sandstone member (lower third) of San Hipólito For- mation. Lithology same as for SH-412-14 (above). Sample from a tan, micritic limestone bed 6.3 cm (2.5 in) thick. 303.1 m (994.2 ft) above the base of the sandstone member. Punta San Hipólito; type locality of San Hipólito Formation. Upper Pliensbachian; ?Toarcian. BPW-30*. —Sandstone member (lower third) of San Hipólito For- mation. Lithology same as for SH-412-14 (above). Sample a me- dium-gray, slightly silty, micritic limestone bed 5 cm (2 in) thick. Approximately 345 m (1131.6 ft) above base of sandstone member. Punta San Hipólito; type locality of the San Hipólito Formation. Upper Pliensbachian; ?Toarcian. TAMAN-TAMAZUNCHALE AREA, SAN Luis Porosí, EAST-CENTRAL MEXICO Upper Jurassic MX-80-20. — Middle portion of lower, more massively-bedded part of Taman Formation. Medium-bedded, dark-gray, micritic limestone with ammonites, abundant Aulacomyella Furlani, 1910, and abundant calcified Radiolaria. 0.1 km (0.06 mi) west of kilo- meter post km 265 on Route 85 (Mexico, D.F.—Nuevo Laredo highway). An ammonite submitted to Dr. Ralph W. Imlay (U. S. Geological Survey, Washington, DC; report on referred fossils, Nov. 1980) was said to greatly resemble Subneumayria profulgens (Burck- hardt, 1906) of “middle Kimmeridgian" age. Imlay noted, however, that this ammonite was too poorly preserved for definite identifi- cation. Loc. MX-80-20 is also situated 1.9 km (1.1 mi) east-northeast of La Cuesta, where Burckhardt (in Heim, 1926) noted Aulacomyella Furlani, 1910, and Glochiceras fialar (Oppel, 1858) (= upper Kim- meridgian sensu gallico). MX-82-3.— Middle portion of lower, more massively-bedded part of Taman Formation. Platy, thin-bedded, dark-gray, micritic lime- stone with medium-bedded, dark-gray, micritic limestone. Sample containing well-preserved, silicified Radiolaria from platy, thin-bed- ded limestone. Above the first occurrence of Aulacomyella Furlani, 1910, in the Taman Formation. Just west of km 266 on Route 85 (Mexico, D.F.—Nuevo Laredo highway). This horizon lies below *The presence of Canoptum anulatum Pessagno and Poisson, 1981, Gorgansium morganense Pessagno and Blome, 1980, and Tril- lus elkhornensis Pessagno and Blome, 1980, in the radiolarian as- semblage from this locality and the other localities cited above sug- gests that these strata are no older than late Pliensbachian. The absence of Zartus jurassicus Pessagno and Blome, 1980, probably indicates a late Pliensbachian rather than a Toarcian age. the first appearance of Mirifusus Pessagno, 1977a, at loc. MX-82-8 and hence, is tentatively assigned to uppermost Zone 1 (sensu Pes- sagno, Blome, and Longoria, 1984). The presence of Aulacomyella at somewhat lower stratigraphic horizons indicates that the strata at loc. MX-82-3 are no older than the /doceras Zone of Cantu Chapa (1971) (= latest early Kimmeridgian). In Mexico, Aulacomyella ranges from the Idoceras Zone to the Virgatosphinctes mexicanus—Aula- comyella neogeae Zone of Cantu Chapa (1971) (lower Kimmeridgian to upper Tithonian [see p. 19]). In conclusion, strata at loc. MX-82- 3 may either be correlative with the /doceras Zone (uppermost lower Kimmeridgian) or with the Glochiceras gp. fialar Zone (upper Kim- meridgian). The radiolarian assemblage still lacks Parvicingula Pes- sagno s. s. (forms with tubular structure on final post-abdominal chamber). In California Parvicingula s. s. first appears in upper Kim- meridgian strata assignable to the upper part of Zone 2 (Locs. JP-1, SA-108, SA-109, NSF-907). MX-82-6.— Middle portion oflower, more massively-bedded part of Taman Formation. Thin-bedded, reddish-weathering, dark-gray, micritic limestone interbedded with medium-bedded, dark-gray, mi- critic limestone. Sample from thin-bedded limestone containing well- preserved silicified Radiolaria. Above loc. MX-82-3 and below loc. MX-82-8 in section. Approximately 45 m (150 ft) west of km 266 on Route 85 (Mexico, D.F.—Nuevo Laredo highway); about 6 km (3.7 mi) east of village of Taman. Upper part of Zone 1 (?). Below first occurrence of Mirifusus Pessagno, 1977a. Upper part of lower Kimmeridgian Idoceras Zone of Cantu Chapa, 19712; probably low- er part of upper Kimmeridgian (Glochiceras gp. fialar Zone of Cantu Chapa, 1971). MX-82-8.— Middle portion of lower, more massively-bedded part of Taman Formation. Predominantly medium-bedded, dark-gray micritic limestone with occasional thin beds (10.2 cm [4 in] to 20.3 cm [8 in]). Samples bearing well-preserved, silicified Radiolaria from adjacent 10.2 cm and 20.3 cm beds. Adjacent to and slightly east of km 266 on Route 85 (Mexico, D. F. Nuevo Laredo highway); 6 km east-northeast of village of Taman. First apparent occurrence of Mirifusus Pessagno, 1977a. Apparent base of Zone 2. Upper part of lower Kimmeridgian (Zdoceras Zone; Cantu Chapa, 1971) or lower part of upper Kimmeridgian (Glochiceras gp. fialar Zone; Cantu Chapa, 1971). Probably upper Kimmeridgian. Below first occurrence of Parvicingula Pessagno s. s. (upper part of Zone 2; upper Kim- meridgian). MX-82-15.—Upper part of lower, more massively-bedded por- tion of Taman Formation. Dark-gray, medium-bedded, micritic limestone with interbedded shale containing limestone nodules. In- determinate ammonites, Aulacomyella sp., and well-preserved Ra- diolaria occur in limestone nodules. Radiolaria replaced by pyrite and limonite. Above first occurrence of Parvicingula Pessagno s. s. (forms with post-abdominal tubes). Upper Zone 2; upper Kimmer- idgian. Route 85 (Mexico, D.F.—Nuevo Laredo highway); just east of km 267 and west of major turn in road. MX-82-16.—Upper part of lower, more massively-bedded part of Taman Formation. Dark-gray micritic, medium-bedded lime- stone with interbedded shale containing limestone nodules with silic- ified Radiolaria. Same horizon as loc. MX-82-15. Route 85 (Mexico, D.F.—Nuevo Laredo highway); east of km 267 and east of major turn in road. Upper Zone 2; upper Kimmeridgian (sensu gallico). MX-82-17.—Upper part of lower, more massively-bedded part of Taman Formation. Dark-gray, medium-bedded, micritic lime- stone with interbedded shale containing limestone nodules. Lime- stone nodules with well-preserved, pyritized Radiolaria. Route 85 (Mexico, D. F. Nuevo Laredo highway); west of km 268 and about 0.8 km (0.5 mi) west of hanging bridge over Río Moctezuma at Village of La Vega (= La Vega Larga of some maps). Zone 3; lower Tithonian. Within the Virgatosphinctes mexicanus-Aulacomyella 52 BULLETIN 326 neogeae Zone of Cantu Chapa (1971). Overlying strata of lower, more massively-bedded Taman still with Aulacomyella Furlani, 1910. MX-81-54.—Upper part of lower, more massively-bedded part of Taman Formation. Dark-gray, micritic, medium-bedded lime- stone with interbedded shale containing limestone nodules. Sample from small limestone nodule with well-preserved, pyritized Radi- olaria. Route 85 (Mexico, D.F.—Nuevo Laredo highway) west of km 268; 0.77 km (0.48 mi) west of hanging bridge over Rio Moc- tezuma at village of La Vega (= La Vega Larga of some maps), 0.48 km west of km 268. Zone 3; lower Tithonian. Close to final occur- rence of Aulacomyella and top of Virgatosphinctes mexicanus—Au- lacomyella neogeae Zone of Cantu Chapa (1971). MX-82-19.— Upper part of lower, more massively-bedded part of Taman Formation. Dark-gray, medium-bedded, micritic lime- stone with interbedded shale. Shale and limestone both containing limestone nodules. Sample a large, dark-gray, micritic limestone nodule from platy limestone layer about 30.4 cm (1 ft) thick; con- taining well-preserved pyritized Radiolaria. 20 m (65.5 ft) below the first occurrence of hyaline calpionellids (= base of upper Tithonian; sensu Pessagno, Blome, and Longoria, 1984). Route 85 (Mexico, D.F.—Nuevo Laredo highway) west of km 268; 0.76 km (0.45 mi) west of hanging bridge over Rio Moctezuma at village of La Vega (= La Vega Larga of some maps). Zone 3; lower Tithonian; upper part. Upper part of Virgatosphinctes mexicanus—Aulacomyella neo- geae Zone of Cantu Chapa (1971). MX-82-20.—Upper part of lower, more massively-bedded part of Taman Formation. Dark-gray, medium-bedded, micritic lime- stone with interbedded shale containing limestone nodules. Lime- stone nodules with well-preserved, pyritized Radiolaria. 10 m (32.8 ft) above loc. MX-82-19; 10 m (32.8 ft) below the first occurrence of hyaline calpionellids in the lower, massively-bedded part of Ta- man Formation. Route 85 (Mexico, D.F.— Nuevo Laredo highway). Zone 3 (upper part); lower Tithonian. Upper part of Virgatosphinctes mexicanus—Aulacomyella neogeae Zone of Cantu Chapa (1971). Au- lacomyella neogeae Imlay, 1940, occurs in the lower Taman just below its contact with the upper Taman near km 268. It also has been observed in the lower part of the upper Taman (see loc. MX- 85-35 below). MX-85-35.—Lower part of thin-bedded upper Taman (= lower Pimienta of Cantu Chapa, 1971; see Pessagno, Longoria, MacLeod, and Six, in press). Thin-bedded, black to dark-gray micritic lime- stone with thin beds of yellowish-weathering shale containing large limestone nodules. 30 m (96.8 ft) above contact with massively- bedded lower Taman. Immediately north of new highway bridge over Rio Moctezuma connecting Taman (San Luis Potosi) on south side of river with Barrio de Guadalupe (San Luis Potosi) on north side of river. Exposure on east side of Barrio de Guadalupe along new road. East limb of tightly-folded synclinal structure, which is overturned to the east. 20 cm (8 in) dark-gray, micritic limestone nodule containing Aulacomyella neogeae Imlay, 1940, and Salinites grossicostatum (Imlay, 1939). Radiolaria assignable to the lower part of Zone 4 (sensu Pessagno, Blome, and Longoria, 1984) occur above and below this horizon. This succession is discussed in more detail by Pessagno, Longoria, MacLeod, and Six, in press). MX-82-37.— Middle portion of thin-bedded, upper part of Taman Formation (= lower Pimienta of Cantu Chapa, 1971). Thin-bedded, black to dark-gray micritic limestone with thick beds of black, yel- lowish-weathering shale containing abundant, black, micritic, fist- sized limestone nodules with well-preserved Radiolaria. Upper Ta- man strata occurring in axial zone of tight synclinal fold noted at loc. MX-85-35 above. About 72 m (239 ft) above loc. MX-85-35 (see above). 0.94 km (0.6 mi) from new highway bridge over Rio Moctezuma on road above Barrio de Guadalupe (San Luis Potosi). REFERENCES CITED Arkell, W. J., Kummel, B., and Wright, C. W. 1957. Mesozoic Ammonoidea, pp. L80-L437, in Moore, R. C. (ed.), Treatise on Invertebrate Paleontology Part L, Mol- lusca 4. Geol. Soc. Amer. and Univ. of Kansas Press. Bandy, O. L. 1951. Upper Cretaceous foraminifera from the Carlsbad area, San Diego County, California. J. Paleontol., vol. 25, No. 4, pp. 488-513, pls. 72-75. Barnes, D. A. 1982. 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Page Kolumbusispeciesp EI oo uere “...!... ucc X sca 21 Lower part of Hyde Formation. loc. OR-600. Lower Jurassic (upper Pliensbachian?; lower Toarcian; upper Toarcian?). 1. Scale bar = 61.2 um. 16. Illustration at higher magnification; showing primary and secondary lateral bars each connected directly with infacing ridge of a given foot (white arrow). We have not observed this relationship on other specimens of Rolumbus, n. gen., or Farcus, n. gen. However, specimens of Rolumbus and Farcus (figs. 11, 12) do show a definite alignment of the four lateral elements with the feet. In this case, there is no direct structural connection between the lateral elements and the feet. Scale bar — 14.1 um. VVV!!! dd!!! NE MC cem SE 26 Warm Springs Member, Snowshoe Formation. loc. OR-589. Lower Jurassic (upper Toarcian). Note tubular velum-like structure extending from base of thorax. Scale bar = 150 um. C!!!) m-DmmDqꝶęq d ß 8 23 Warm Springs Member, Snowshoe formation. loc. OR-589. Lower Jurassic (upper Toarcian). Note alignment of four feet with primary and secondary lateral elements. Figure 18 shows cephalic skeletal elements. Terminology follows that of Goll (1968, p. 1413) and Pessagno (1969, pl. 24). Note that the dorsal bar is absent; compare with figures 15 and 17. Collar pores blackened in figure 18 to increase contrast. Scale bar = 59, 37.5, and 15 um, respectively. , MM Dꝓꝶq?̃t HP c xcu ux 29. 30 Upper part of South Fork Member, Snowshoe Formation. loc. OR-501B. Middle Jurassic (upper Bathonian). Arrows (fig. 4) point to one of four A-frames. Figure 6 shows circular aperture bordered by an imperforate rim; area between rim and base of A-frame comprised of latticed meshwork. Note two layers of abdomen (fig. 10); outer latticed layer formed of vermicular ridges. Scale bar = 84, 39, 75, and 54 um, respectively. Unnamed dicyrtid nasselaran (aliran aponi di) WM two teet TU 8 32 South Fork Member, Snowshoe Formation. loc. OR-501B. Middle Jurassic (upper Bathonian). Arrow points to cephalocone. Scale bar = 120 um. ELN LEE 시조 기 te EN Spe wl eg ee ee 32 South Fork Member, Snowshoe Formation. loc. OR-501B. Middle Jurassic (upper Bathonian). Note that the pore frames inside of the test are flattened and low in relief whereas those on the outside of test are high in relief. Figure 15 shows cephalic skeletal elements. A dorsal bar is present among species of Napora Pessagno, 1977a. However, it is lacking with species of Hilarisirex Takemura and Nakaseko, 1982, Farcus, n. gen., and Rolumbus, n. gen. Apical bar not shown in this view. Scale bar — 60 and 30 um, respectively. 777; E doe uuu o E 30 South Fork Member, Snowshoe Formation. loc. OR-501B. Middle Jurassic (upper Bathonian). Note absence of dorsal bar among cephalic skeletal elements. Scale bar — 39 um. FAV CUSISPECICS wo onum cete q ̃ dd!!! ß I MM 23 Lower part of Hyde Formation. loc. OR-600. Lower Jurassic (upper Pliensbachian?; lower Toarcian; upper Toarcian?). Figure 14 shows cephalic skeletal elements. Note absence of dorsal bar. Scale bar — 40 and 15 um, respectively. GEEDHAPISIFEXSSDCCIOSR TE qe 시소 NE c Sox eet Ge ITE c Pe E M HUM tuu aa ee 30 South Fork Member, Snowshoe Formation. loc. OR-501B. Middle Jurassic (upper Bathonian). Note thorax (T) and absence of dorsal bar among cephalic skeletal elements. Scale bar = 30 um. Ne eater, a n m v n Le o Mm. 30‏ ری ار ار تا Topotype. South Fork Member, Snowshoe Formation. loc. OR-501B. Middle Jurassic (upper Bathonian). Arrow points to imperforate shelflike partition separating thorax from abdomen at top of A-frames. Circular aperture (mouth) at base of abdomen is like that described in figure 6. Scale bar — 37.5 um. 58 BULLETIN 326 EXPLANATION OF PLATE 2 All figures are scanning electron micrographs of ultranaporid and farcid Nassellariina from the Lower Jurassic Kunga and Maude formations, Queen Charlotte Islands, British Columbia; and the Nicely Formation, east-central Oregon. Scale bar (upper right) is used as a reference for the magnification of all figures. Figure 1-3, 10, 11, 14. 4, 6-8, 12, 15. „„ Napora (2) graybayensis, new ۹066168 ed Black argillite member, Kunga Formation, Queen Charlotte Islands. 1, 10, 14. Holotype (USNM 379327). loc. QC-675; upper Sinemurian. Scale bar = 48, 30, and 38 um, respectively. 2, 11. Paratypes (Pessagno Collection). loc. QC-675; upper Sinemurian. Scale bar = 58.8 and 30 um, respectively. 3. Paratype (Pessagno Collection). loc. QC-675; upper Sinemurian. Scale bar = 54 um. Farcus graylockensis, new specie hel en eee eee ipe dre hi ye etie sert seiten Nicely Formation, east-central Oregon. 6, 7, 15. Holotype (USNM 379278). loc. OR-536; upper Pliensbachian. Scale bar — 84 and 150 um. 4, 8, 12. Paratype (Pessagno Collection). loc. OR-536; upper Pliensbachian. Scale bar — 99, 75, and 75 um, respectively. 00006 (2) sandspitensts) ß . Maude Formation, Queen Charlotte Islands. 5, 16, 17. Paratype (Pessagno Collection). loc. QC-534; lower Pliensbachian. Scale bar = 120, 60, and 30 um, respectively. 9. 13. Holotype (USNM 379294). loc. QC-534; lower Pliensbachian. Scale bar — 99 and 60 um, respectively. BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 91 BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 91 PLATE 3 YE 22570 TAZA A igh ee EN, EF JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 59 EXPLANATION OF PLATE 3 All figures are scanning electron micrographs of farcid and ultranaporid Nassellariina from the Lower Jurassic San Hipölito Formation, Vizcaino Peninsula, Baja California Sur, Mexico; the Franciscan Complex, California; and the Nicely Formation, east-central Oregon. Scale bar (upper right) is used for the magnification of all figures. Figure Page و0 رل‎ Sol e, DO WISDEOIOS E er e ie, ten en yT 28 Sandstone member, San Hipölito Formation. 1, 18. Holotype (USNM 379353). loc. SH-412-14; upper Pliensbachian; ?Toarcian. Scale bar = 88.2 and 42.8 um, respectively. 6, 19. Paratype (Pessagno Collection). loc. SH-412-14; upper Pliensbachian; ?Toarcian. Scale bar = 83.7 and 46.5 um, respectively. 2. 0006 CY Species ab J COY Sanas prient Dew SPECS y RUIN 33 Red ribbon cherts, Franciscan Complex. loc. NSF-960; lower Pliensbachian?; upper Pliensbachian. Scale bar = 84 um. 3 SLO LL loss Naporasmorganensisunew.Speciesp were os d ß ß NG 43 Nicely Formation. Upper Pliensbachian. 3, 8, 11. Holotype (USNM 379343). loc. OR-536. Scale bar = 120, 84, and 99 um, respectively. 10, 15. Paratype (Pessagno Collection). loc. OR-536. Scale bar = 84 and 99 um, respectively. da Kürcusispeciest !!!.... A 24 Nicely Formation. loc. OR-536; upper Pliensbachian. Scale bar — 107 um. , REN SBE TC EE 26 Nicely Formation. 5. Holotype (USNM 379282). loc. OR-536; upper Pliensbachian. Scale bar = 99 um. 7,9, 11. Paratypes (Pessagno Collection). loc. OR-536; upper Pliensbachian. Scale bar = 99, 120, and 84 um, re- spectively. D, 16. 17; 217 Kareus:asperoensisunewaspecies..... de ecc Se EE 23 Sandstone member, San Hipölito Formation. 12, 17, 21. Holotype (USNM 379276). loc. SH-412-14; upper Pliensbachian; ?Toarcian. Scale bar = 61.2, 30, and 31.6 um, respectively. 16. Paratype (Pessagno Collection). loc. SH-412-14; upper Pliensbachian; ?Toarcian. Scale bar — 72 um. I3 durus species BT comune e M TEE ß NE 24 Nicely Formation. loc. OR-536; upper Pliensbachian. Scale bar — 85.5 um. 20: YJacHs:()°SPECIESLE. Mn m E I M M M NC A e E 34 Sandstone member, San Hipólito Formation. loc. SH-412-14; upper Pliensbachian; ?Toarcian. Scale bar — 61.2 um. 60 BULLETIN 326 EXPLANATION OF PLATE 4 All figures are scanning electron micrographs of farcid and ultranaporid Nassellariina from the Lower Jurassic part of the San Hipölito Formation, Vizcaino Peninsula, Baja California Sur, Mexico. Scale bar (upper right) is used as a reference for the magnification of all figures. Figure Page 1:5 09 Po OLDS DOSES We SDC P lll ß 8 26 Sandstone member, San Hipölito Formation. 1, 6, 12, 14. Paratype (Pessagno Collection). loc. BPW-30; upper Pliensbachian; ?Toarcian. Scale bar = 88.2, 88.2, 40, and 30 um, respectively. 5, 9, 13. Holotype (USNM 379280). loc. BPW-30; upper Pliensbachian; ?Toarcian. Scale bar = 88.2, 40, and 40 um, respectively. ان‎ ELE 38 Sandstone member, San Hipólito Formation. 2, 10. Holotype (USNM 379321). loc. BPW-30; upper Pliensbachian; ?Toarcian. Scale bar = 88.5 and 54 um, respectively. 3, 15; 4, 16. Paratypes (Pessagno Collection). loc. BPW-30; upper Pliensbachian; ?Toarcian. Scale bar — 88.2, 40 um; 87, 40 um, respectively. JJ!!! ß ß 32 Holotype (USMN 379292). Sandstone member, San Hipölito Formation. loc. BPW-30; upper Pliensbachian; ?Toarcian. Scale bar = 81, 54, and 51 um, respectively. BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 91 PLATE 4 ON n = - "| (S > 5 E Z O D e < A 2 < = 2 eat = < A un 2 = m = — 2۵ JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 61 EXPLANATION OF PLATE 5 | All figures are scanning electron micrographs of ultranaporid and farcid Nassellariina from the Lower Jurassic: Maude Formation, Queen Charlotte Islands, British Columbia; Hyde and Snowshoe formations, Grant County, east-central Oregon; and San Hipólito Formation, Vizcaino Peninsula, Baja California Sur, Mexico. Scale bar (upper right) is used as a reference for the magnification of all figures. Figure Page IIS L6; L7 ,, ß e o e RU COD . T E 이 으으 28 1, 16, 17. Holotype (USNM 379284). Hyde Formation. loc. OR-600; upper Pliensbachian?; lower Toarcian; ?upper Toar- cian. Scale bar — 120, 60, and 60 um, respectively. 11. Paratype (Pessagno Collection). Hyde Formation. loc. OR-600; upper Pliensbachian?; lower Toarcian; ?upper Toarcian. Scale bar — 84 um. رت‎ Rolumbussvenustasanewispeuiesne e e dc y d mer M re 32 2, 18. Holotype (USNM 379286). Hyde Formation. loc. OR-600; upper Pliensbachian?; lower Toarcian; ?upper Toar- cian. Scale bar — 99 and 60 um, respectively. 3. Paratype (Pessagno Collection). Hyde Formation. loc. OR-600; upper Pliensbachian?; lower Toarcian; ?upper Toarcian. Scale bar = 99 um. 43 JAGUNG) SSDECIOSEA cos r ʒ ! HT 34 Maude Formation. loc. QC-622; upper Pliensbachian; ?lower Toarcian. Scale bar — 84 um. ! وس ورد‎ e,, , Z...... I M M M EE 41 5. Paratype (Pessagno Collection). Warm Springs Member, Snowshoe Formation. loc. OR-589; upper Toarcian. Scale bar = 99 um. 12, 13. Holotype (USNM 379333). Warm Springs Member, Snowshoe Formation. loc. OR-589; upper Toarcian. Scale bar — 84 and 60 um, respectively. 6; I4:-Jacus;refelenstesnew.Speclese c edv ot E EREMO MI LM I M 32 Paratype (Pessagno Collection). Sandstone member, San Hipólito Formation. loc. BPW-30; upper Pliensbachian; ?Toarcian. Scale bar — 87 and 40 um, respectively. T$ 0: LANU SPEI EO n . EE 24 Sandstone member, San Hipólito Formation. loc. BPW-30; upper Pliensbachian; ?Toarcian. Scale bar = 87 and 61.2 um, respectively. 8 10. NGDOFO IEG . yd dd!!! cx. 42 Holotype (USNM 379339). Hyde Formation. loc. OR-600; upper Pliensbachian?; lower Toarcian; ?upper Toarcian. Scale bar — 120 and 54 um, respectively. e o yd d uc uL I 34 Warm Springs Member, Snowshoe Formation. loc. OR-589; upper Toarcian. Scale bar = 75 um. 62 BULLETIN 326 EXPLANATION OF PLATE 6 All figures are scanning electron micrographs of ultranaporid Nassellariina from the Middle Jurassic (Aalenian? and lower Bajocian) Snowshoe Formation, Grant County, east-central Oregon. Scale bar (upper right) is used as a reference for the magnification of all figures. Figure 1-3. I; 135515 19, 22-24. 12; 14-17. 1821. 16, 20. Napora fructuosa, new specie ? Warm Springs Member, Snowshoe Formation. This species is also known from the Lower Jurassic (upper Toarcian). 1. Holotype (USNM 379325). loc. OR-593; ?Aalenian. Scale bar = 109 um. 2, 3. Paratypes (Pessagno Collection). loc. OR-593; ?Aalenian. Scale bar = 120 and 99 um, respectively. ! y y Duce ende Ld es et: Warm Springs Member, Snowshoe Formation. 4. Holotype (USNM 379302). loc. OR-580; ?Aalenian. Scale bar = 75 um. 5. Topotype (destroyed in SEM work). loc. OR-580; ?Aalenian. Arrow points to cephalocone. Cephalis is quite large. Scale bar — 75 um. / wae eee eis tis tee MD Up eue Tm Sidus uec e Warm Springs Member, Snowshoe Formation. 6. Holotype (USNM 379306). loc. OR-580; ?Aalenian. Arrow points to cephalocone. Cephalis is quite large. Scale bar = 99 um. 7. Paratype (Pessagno Collection). loc. OR-580; ?Aalenian. Arrow points to cephalocone. Note large cephalis and asymmetrical horn. Scale bar — 109 um. . Napora species aff. N. cosmica, new species Warm Springs Member, Snowshoe Formation. loc. OR-580; ?Aalenian. Scale bar = 99 um. NADO ODI CIO y d r Warm Springs Member, Snowshoe Formation. This species differs from N. fructuosa, n. sp., by having a longer horn with wider grooves and a smaller cephalis. 9. Holotype (USNM 379349). loc. OR-555; lower Bajocian. Scale bar = 120 um. 10. Paratype (Pessagno Collection). loc. OR-555; lower Bajocian. Scale bar = 120 um. Napora baumgartneri, new Species ęↄ nee tees 11, 19, 22. Holotype (USNM 379298). Warm Springs Member, Snowshoe Formation. loc. OR-554; lower Ba- jocian. Scale bar = 84, 66, and 42 um, respectively. 13, 24. Figured Specimen. Warm Springs Member, Snowshoe Formation. loc. OR-594; lower Bajocian. Scale bar = 99 and 45 um, respectively. 15, 23. Paratype (Pessagno Collection). Warm Springs Member, Snowshoe Formation. loc. OR-554; lower Bajocian. Scale bar = 108 and 48 um, respectively. d NU COL Grune uD dM u a Warm Springs Member, Snowshoe Formation; loc. OR-593; ?Aalenian. Scale bar = 99 um. Napora opaca- new species na. t Warm Springs Member, Snowshoe Formation. 14, 18. Holotype (USNM 379345). loc. OR-594; lower Bajocian. Scale bar = 99 and 45 um, respectively. 17, 21. Paratype (Pessagno Collection). loc. OR-594; lower Bajocian. Scale bar — 99 and 48 um, respectively. EEN Warm Springs Member, Snowshoe Formation. 16. Paratype (Pessagno Collection). loc. OR-555; lower Bajocian. Arrow points to massive cephalocone. Scale bar = 99 um. 20. Holotype (USNM 379331). loc. OR-555; lower Bajocian. Arrow points to massive cephalocone. Note large cephalis and massive, asymmetrically-placed horn. Scale bar = 84 um. — O = 2 E — ^ > s ALEONTOLOGY BERLIN. Fn BULLETINS OF AMERICAN P BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 91 JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 63 EXPLANATION OF PLATE 7 | All figures are scanning electron micrographs of Middle Jurassic ultranaporid and hilarisiregid Nassellariina from the Snowshoe Formation, Grant County, east-central Oregon. Scale bar (upper right) is used as a reference for the magnification of all figures. Figure 120: 291, 19, 21, 22. 3547195123. SE SIC CTC AL E ey ee DEM lU CT tL M UM 3I Warm Springs Member, Snowshoe Formation, near Izee. loc. OR-594; lower Bajocian. Note outer latticed layer of vermicular ridges. Scale bar = 150 and 54 um, respectively. JNODOFGICOSIHICU DS NES DECIES 에조 A cM M M C ue eae 38 South Fork Member, Snowshoe Formation. 2, 7T. Holotype (USNM 379323). loc. OR-513; upper Bajocian. Scale bar — 69 and 84 um, respectively. 5, 6, 19, 22. Paratype (Pessagno Collection). loc. OR-513; upper Bajocian. Scale bar — 84, 84, 60, and 40 um, respectively. 21. Paratype (Pessagno Collection). loc. OR-513; upper Bajocian. Scale bar = 30 um. dd y y y SENE E I E E 42 Warm Springs Member, Snowshoe Formation. 3, 4. Paratypes (Pessagno Collection). loc. OR-555; lower Bajocian. Scale bar = 109 and 171 um, respectively. 13, 23. Holotype (USNM 379337). loc. OR-555; lower Bajocian. Note long, straight feet, which distinguish this species from N. baumgartneri, n. sp. (see Pl. 6, fig. 11) and N. opaca, n. sp. (see Pl. 6, fig. 14). Scale bar — 99 and 60 um, respectively. ff!!! BE Mm ! ß m M T 46 Lower part of Warm Springs Member, Snowshoe Formation. loc. OR-516; lower Bajocian. Scale bar — 48 um. CJ ...!... i E 46 Snowshoe Formation (undifferentiated), exposed near Seneca. loc. OR-550C; upper Bajocian. Scale bar — 60 um. DECS M DNE DI UU MIO OMNE d a ME ME 35‏ مرها هدر لب ابر زر تا Snowshoe Formation (undifferentiated) exposed near Seneca. 10, 12. Paratypes (Pessagno Collection). loc. OR-549B; upper Bajocian. Scale bar — 99 and 99 um, respectively. 11. Holotype (USNM 379300). Note large cephalocone. loc. OR-549B; upper Bajocian. Scale bar = 99 um. ۱ ۱۷۵۵۹۱۵0 NES c ...... cc eee ee 46 Warm Springs Member, Snowshoe Formation. loc. OR-554; lower Bajocian. Scale bar = 60 um. d e ed NER uu ß Mu qu a 32 Snowshoe Formation (undifferentiated) exposed near Seneca. loc. OR-549B; upper Bajocian. Scale bar — 99 um. o LLUN TONES DECIS ADA a oS as IUS EAD M UD T ee 32 Warm Springs Member, Snowshoe Formation. loc. OR-554; lower Bajocian. Scale bar — 75 um. C“ ll! m. 88 51 South Fork Member, Snowshoe Formation exposed near Izee (see also Pl. 8). 17. Holotype (USNM 379290). loc. OR-501B; upper Bathonian. Note inner latticed layer of flattened po- lygonal pore frames and outer latticed layer of vermicular ridges comprising abdominal wall. Scale bar — 84 um. 18. Paratype (Pessagno Collection). loc. OR-501B. Note that outer latticed layer of vermicular ridges is more highly-developed on this specimen than on the holotype (Pl. 7, fig. 17). Scale bar = 99 um. BULLETIN 326 EXPLANATION OF PLATE 8 All figures are scanning electron micrographs of Middle Jurassic (upper Bathonian) ultranaporid and hilarisiregid Nassellariina. Scale bar (upper right) is used as a reference for the magnification of all figures. Figure ,, . d N GS O DG CO 41 South Fork Member, Snowshoe Formation, near Izee, Grant County, Oregon. 1, 8, 16. Holotype (USNM 379335). loc. OR-501B; upper Bathonian. Scale bar = 171, 54, and 54 um, re- spectively. 7. Paratype (Pessagno Collection). loc. OR-501B; upper Bathonian. Scale = 132 um. 9. Paratype (Pessagno Collection). loc. OR-501B; upper Bathonian. Scale bar = 150 um. 11. Paratype (Pessagno Collection). loc. OR-501B; upper Bathonian. Scale bar = 99 um. 2.3.19, 20-93, Napormantelopensiw:ew:Spectes a m EE 34 South Fork Member, Snowshoe Formation, near Izee, Grant County, Oregon. 2, 15, 22, 23. Holotype (USNM 379296). loc. OR-501B; upper Bathonian. Scale bar = 99, 75, 48, and 48 um, respectively. 3, 20, 21. Paratype (Pessagno Collection). loc. OR-501B; upper Bathonian. Scale bar = 99, 48, and 48 um, respectively. 495. 10, 13. , ę q q hg t m S Un E ine ra eer 30 South Fork Member, Snowshoe Formation, near Izee, Grant County, Oregon. 4, 5, 17. Holotype (USNM 379288). loc. OR-501B; upper Bathonian. Scale bar = 99, 109, and 48 um, re- spectively. 6, 14. Topotype. loc. OR-501B; upper Bathonian. Specimen destroyed during SEM work. On abdomen, note flattened pore frames comprising inner latticed layer and weakly-developed vermicular outer latticed layer. Scale bar — 99 and 60 um, respectively. 10, 13. Paratypes (Pessagno Collection). loc. OR-501B; upper Bathonian. See comments on morphology for figures 6 and 14 above. Scale bar = 84 and 48 um, respectively. 12. 18, 19. -Hilarisirex oregonensis, EE 31 South Fork Member, Snowshoe Formation, near Izee, Grant County, Oregon. 12. Paratype (Pessagno Collection). loc. OR-501B; upper Bathonian. Scale bar = 84 um. 18. Holotype (USNM 379290). loc. OR-501B; upper Bathonian (see also Pl. 7, fig. 17). Scale bar = 48 um. 19. Paratype (Pessagno Collection). loc. OR-501B; upper Bathonian (see also Pl. 7, fig. 18). Scale bar = 48 um. BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 91 BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 91 PLATE 9 JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 65 EXPLANATION OF PLATE 9 All figures are scanning electron micrographs of Middle Jurassic ultranaporid Nassellariina from Oregon and Upper Jurassic ultranaporid Nassellariina from California and Mexico. Scale bar (upper right) is used as a reference for the magnification of all figures. Figure Page 552: 18218 ae NADOPAREUINE LEU OSU ß We sets oe ea a tn UE ß M y. 44 South Fork Member, Snowshoe Formation, near Izee, Grant County, Oregon. Middle Jurassic. 1. Paratype (Pessagno Collection). loc. OR-501B; upper Bathonian. Scale bar = 133 um. 2. Holotype (USNM 379347). loc. OR-501B; upper Bathonian. Scale bar = 120 um. 7, 18. Paratype (Pessagno Collection). loc. OR-501B; Upper Bathonian. Note flattened pore frames on thoracic interior. Scale bar = 99 and 66 um, respectively. S; e Napara LON MMDꝓꝶq7qf¼qꝓñtc0 d y Se Bree 36 Lower member oftype Taman Formation west of Tamazunchale, San Luis Potosí, Mexico. Upper Zone 2 (sensu Pessagno, Blome, and Longoria, 1984). 3, 17, 23. Holotype (USNM 379304). loc. MX-82-15; upper Kimmeridgian. Note distinctive horn. Specimen replaced by limonite. Scale bar — 100, 58.8, and 37.5 um, respectively. 4, 19. Paratype (Pessagno Collection). Specimen replaced by limonite. Scale bar — 100 and 37.5 um, respectively. SIZE. Napara DURT ESSIEN Ta Pc WEN Nu Wel ñ⁊ñ y d UL ILS 8 37 Volcanogenic-pelagic strata overlying Coast Range ophiolite at Point Sal, Santa Barbara County, California. Upper Jurassic. 5. Holotype (USNM 22002). loc. NSF-907; upper Kimmeridgian. Note figured specimen is foreshortened due to tilting. Thorax normally appears more hemispherical in character. Scale bar = 60 um. 12. Figured specimen. loc. NSF-908; lower Tithonian; Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). C (arrow) marks cephalocone. Scale bar = 60 um. 13, 14. Topotype. loc. NSF-907; upper Kimmeridgian; upper Zone 2 (sensu Pessagno, Blome, and Longoria, 1984). Scale bar = 99 and 99 um, respectively. 6-15. Napora species all. N. mo6tezumaensisunewaspeciesar ee UAE 43 Lower member of type Taman Formation west of Tamazunchale, San Luis Potosí, Mexico. loc. MX-82-8. Upper Jurassic (lower part of upper Kimmeridgian). Lower Zone 2 (sensu Pessagno, Blome, and Longoria, 1984). Scale bar = 85.5 and 37.5 um, respectively. 8510: 20-22. INaporamoctezumdensis; newiSpeoleS?u ðᷣ EE 43 Lower member of type Taman Formation west of Tamazunchale, San Luis Potosí, Mexico. Upper Jurassic. Lower part of Zone 2 (sensu Pessagno, Blome, and Longoria, 1984). 8. Paratype (Pessagno Collection). loc. MX-82-8; lower part of upper Kimmeridgian. Note slender feet and distinctive horn (Pl. 9, figs. 20, 21). Scale bar = 85.5 um. 9, 20. Paratype (Pessagno Collection). loc. MX-82-8. Scale bar — 85.5 and 37.5 um, respectively. 10, 22. Holotype (USNM 379341). loc. MX-82-8; upper Kimmeridgian. Scale bar — 85.5 and 37.5 um, respectively. 21. Paratype (Pessagno Collection). loc. MX-82-8; lower part of upper Kimmeridgian. Scale bar — 58.8 um. ] 1, 16. ß oes eeu ..... M E Am ea 42 Volcanogenic-pelagic strata overlying Coast Range ophiolite at Point Sal, Santa Barbara County, California. Upper Jurassic. Upper Zone 2 (sensu Pessagno, Blome, and Longoria, 1984). 11. Holotype (USNM 22004). loc. NSF-907. Note broad thorax, massive pore frames, massive short horn, and massive short feet; feet broken. Scale bar — 60 um. 16. Topotype. Pore frames more massive and less numerous than those of holotype. loc. NSF-907; upper Kim- meridgian. Scale bar — 48 um. 24 e / y EE iUe (ah Mu e Ba as MH 45 Lower member of type Taman Formation west of Tamazunchale, San Luis Potosí, Mexico. Upper Jurassic. Lower Zone 2 (sensu Pessagno, Blome, and Longoria, 1984). Holotype (USNM 379351). loc. MX-82-8; upper Kimmeridgian. Note long, massive, straight feet, and short, massive horn. Scale bar = 85.5 um. 66 BULLETIN 326 EXPLANATION OF PLATE 10 All figures are scanning electron micrographs of Upper J urassic (upper Kimmeridgian to upper Tithonian) hilar- isiregid and ultranaporid Nassellariina from California and east-central Mexico. Scale bar (upper right) is used as a reference for the magnification of all figures. Figure Le 2-5, 15, 16, 21-23. — 8, 10-12, 17, 20, 24. 18. A d Volcanogenic-pelagic strata overlying Coast Range ophiolite at Point Sal, Santa Barbara County, California. loc. NSF-907; upper Kimmeridgian. Scale bar = 150 um. Napora burckhardti, new ۹66165 ۰۰۰۰۰۰۰۰۰۰۰ aaa Kn yT Lower member of type Taman Formation west of Tamazunchale, San Luis Potosí, Mexico. Upper Jurassic (lower Tithonian). Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). 2, 3, 15, 21. Holotype (USNM 379308). loc. MX-81-54. Note distinctive horn and long, slender feet. Specimen replaced by pyrite. Scale bar = 99, 99, 33, and 42 um, respectively. 4, 16, 22. Paratype (Pessagno Collection). loc. MX-81-54. Specimen replaced by pyrite. Scale bar = 99, 48, and 48 um, respectively. 5. Paratype (Pessagno Collection). loc. MX-81-54. Specimen replaced by pyrite. Scale bar = 99 um. 23. Paratype (Pessagno Collection). loc. MX-81-54. Cephalic wall and upper part of thoracic wall broken away. C marks hemispherical cephalis. Scale bar = 45 um. J .. en Volcanogenic-pelagic strata overlying Coast Range ophiolite at Point Sal, Santa Barbara County, California. loc. NSF-907; upper Kimmeridgian). Upper part of Zone 2 (sensu Pessagno, Blome, and Longoria, 1984). Scale bar = 120 um. NDIO EAEE M2 d c Lower member oftype Taman Formation west of Tamazunchale, San Luis Potosi, Mexico. loc. MX-81-54; lower Tithonian. Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). Specimen replaced by pyrite. Scale bar = 99 um. Napora heimi . w Lower member oftype Taman Formation west of Tamazunchale, San Luis Potosi, Mexico. Upper Jurassic (lower Tithonian). Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). 8, 20, 24. Holotype (USNM 379329). loc. MX-81-54. Note massive horn with large, lenticular grooves between massive, rounded ridges. Specimen replaced by pyrite. Scale bar = 84, 42, and 42 um, respectively. 10. Paratype (Pessagno Collection). loc. MX-81-54. Specimen replaced by pyrite. Scale bar = 84 um. 11. Figured specimen. loc. MX-82-20; replaced by pyrite. Scale bar = 85.5 um. 12, 17. Figured specimen. loc. MX-82-20. Specimen replaced by pyrite. Note structure of horn. Scale bar = 85.5 and 37.5 um, respectively. dd EE Upper member oftype Taman Formation near village of Taman, San Luis Potosi, Mexico. loc. MX-82-37. Upper Jurassic (lower part of upper Tithonian); lower Zone 4 (sensu Pessagno, Blome, and Longoria, 1984). Scale bar = 142 um. . Napora species aff. N. heimi, new species ۰۰۰۰۰۰۰۰۰ nan aa ia rane Waa RT Lower member oftype Taman Formation west of Tamazunchale, San Luis Potosi, Mexico. loc. MX-81-54. Upper Jurassic (lower Tithonian). Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). Specimen replaced by pyrite. Scale bar = 84 um. . Napora deweveri Baumgartner, sensu loo „„ Lower member of type Taman Formation west of Tamazunchale, San Luis Potosí, Mexico. loc. MX-81-54. Upper Jurassic (lower Tithonian). Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). Specimen replaced by pyrite. This form differs from N. deweveri s.s. by having larger, less numerous pore frames and a more hemispherical thorax. Scale bar = 84 um. ed ⁰ HE Upper member of type Taman Formation near village of Taman, San Luis Potosi, Mexico. loc. MX-82-37. Upper Jurassic (lower part of upper Tithonian). Lowermost Zone 4 (sensu Pessagno, Blome, and Longoria, 1984). Scale bar = 85.5 um. . Napora species aff. N. deweveri Baumgartner nnn Lower member oftype Taman Formation west of Tamazunchale, San Luis Potosi, Mexico. loc. MX-82-20. Upper Jurassic (lower Tithonian). Zone 3 (sensu Pessagno, Blome, and Longoria, 1984). Specimen replaced by pyrite. This form differs from N. deweveri s.s. by having a horn with large, lenticular, open grooves. It does possess a subcylindrical thorax with numerous pore frames. Scale bar = 85.5 um. BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 91 PLATE 10 — d E ess we e ua E EN sages > e Im ( y Ze uec. وی( Got? * 8 BULLETINS OF AMERICAN PALEONTOLOGY, VOLUME 91 PLATE 11 JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH EXPLANATION OF PLATE 11 67 All figures are transmitted light photomicrographs of Jurassic Nassellariina. The preservation of most of the Radiolaria was not conducive to transmitted-light microscopy. As a result, only a few taxa could be illustrated using transmitted light photomicrographs. Figure IE: 14. ZTVV)))VJ)V!!! LM. CULO LUN La EE Paratype (USNM 379289). loc. OR-501B. South Fork Member, Snowshoe Formation, east-central Oregon. Middle Jurassic (upper Bathonian). Width of A-frame (base of abdomen) — 110 um. ß EE AS Paratype (USNM 379338). loc. OR-555. Warm Springs Member, Snowshoe Formation, east-central Oregon. Middle Jurassic (lower Bajocian). Length of horn = 60 um. NAROKA APA VUE) ß... E EUER e ON T Paratype (USNM 379328). loc. QC-675. Middle black argillite member, Kunga Formation, Queen Charlotte Islands, B.C. Lower Jurassic (upper Sinemurian). Length of horn of specimen in figure 3 — 60 um; length of horn in specimen in figure 4 — 60 um. Uu NADO HON de OO Was POG CSii S oU CONO RE PRIMNS EE Paratype (USNM 379332). loc. OR-555. Warm Springs Member, Snowshoe Formation, east-central Oregon. Middle Jurassic (lower Bajocian). Length of foot (right) = 100 um. A OTA RONGE WENGI GS N O EL IRR ny Vin MEE a iy Oe S a tM T erg Paratype (USNM 379326). loc. OR-593. Warm Springs Member, Snowshoe Formation, east-central Oregon. Middle Jurassic (Aalenian?). Length of horn = 48 um. e ße. d MM AE I EE. Paratype (USNM 379301). loc. OR-549B. Snowshoe Formation, east-central Oregon. Middle Jurassic (upper Bajocian). Length of horn = 50 um. NAD OR ICONS IS ROV r: NUT E E d Paratype (USNM 379336). loc. OR-501B. South Fork Member, Snowshoe Formation, east-central Oregon. Middle Jurassic (upper Bathonian). Length of horn = 90 um. cu drcus USDEROCNSIS pk... roe e ee te es ta ee, Paratype (USNM 379277). loc. SH-412-14. Sandstone member, San Hipolito Formation, Baja California Sur, Mexico. Lower Jurassic (upper Pliensbachian; Toarcian?). Length of horn = 66 um. NAHH COS HICE SOCIO oir EE A renee ! ID RESULT Paratype (USNM 379324). loc. OR-513. South Fork Member, Snowshoe Formation, east-central Oregon. Middle Jurassic (upper Bajocian). Length of horn = 80 um. e E EE Paratype (USNM 379340). loc. OR-600. Hyde Formation, east-central Oregon. Lower Jurassic (upper Pliensbachian?; lower Toarcian; upper Pliensbachian?). Same specimen viewed at different focal planes. Length of horn = 60 um. ic VACHS: (2) Sara r ee ee qe MM RE Paratype (USNM 379295). loc. QC-534. Maude Formation, Queen Charlotte Islands, B.C. Lower Jurassic (lower Pliensbachian). Length of horn = 55 um. i nt eet EE EEN Hyde Formation, east-central Oregon. Lower Jurassic (upper Pliensbachian?; lower Toarcian; upper Toarcian?). Length of horn = 90 um. e Roluntbus mirus; NOW species... RS ER oe 8 Paratype (USNM 379285). loc. OR-600. Hyde Formation, east-central Oregon. Lower Jurassic (upper Pliensbachian?; lower Toarcian; upper Toarcian?). Longer horn = 95 um. . Napora began ew EE Paratype (USNM 379352). loc. MX-82-8. Taman Formation, east-central Mexico. Upper Jurassic (Kimmeridgian). Length of horn = 45 um. < Napora TAY EIU, NEW , . dU BN een aan ae ale s se nn in ee یه‎ Paratype (USNM 379350). loc. OR-555. Warm Springs Member, Snowshoe Formation, east-central Oregon. Middle Jurassic (lower Bajocian). Length of horn = 55 um. . Napora antelopensis, new Species... vet وی و‎ en ne میم وم‎ 8 Paratype (USNM 379297). loc. OR-501B. South Fork Member, Snowshoe Formation, east-central Oregon. Middle Jurassic (upper Bathonian). Length of horn = 70 um. . Rolumbus mirus; NEW Species: a. aa shin aan Re f . 8 Paratype (USNM 379285). loc. OR-600. Hyde Formation, east-central Oregon. Lower Jurassic (upper Pliensbachian?; lower Toarcian; upper Toarcian?). Longer horn = 100 um. 40 33 Lp 28 45 45 34 28 BULLETIN 326 INDEX Note: Page numbers are in light face, plate numbers are in bold face type; principal discussion pages are in italics; F = foldout inside back cover. Aalen 8, 10, 14,15, 27, 30, 36, 37, 39,4547, 50, F o , ees 17750 Acanthocircus Fe ene, nan eret rere tta 11,19 variabilis (Squinabol, 1914) 50 actaeon, Tropidoceras nn... mdf Ret a cde p em EE BYOO Ks ANAM Re oe ne EE ۳ ان‎ Oe nee nes SC f e e inne de c HUE 8 alpine-Himalayan Belt GIS SO OTE ee A M ² ² my D. qu REIN eff 8 Amaliheus m, Standard one 14 Amoebites Buckman, 1925 Amoeboceras Hyatt, 1900 amphitreptera, Podocapsa antecedens Standard Zone antelopensis, Napora anulatum, Canoptum ... 49,51,F ۲ EE 20 ENEE 19 dd cess cn N ee qui 48 P ESTES BUNGIE d 13 e ße te tetra en 13 , 10,14 , END IE ee een ee 11 JJ. DIE on „ e Pÿfr مه هو‎ RE 47 , 47 e e tr eben ae cr E a HE MIR 20 MABAOS ZONE , 19 U d AG EE 8,10 e EE E EE 8,10 % ß 8,11, 51 ee e oc NS ORD 19:51:57 —˙ ans yong ca lip p ĩ RII D ETT ere ee 48 Baja California Sur 7, 8, 10, 20, 23,24, 26,28, 30, 33, 34, 38, 46,51 We,, esse soon 8,10,20,24,51 Bajoorur aa 5-8,10,14-16,27,30-32,35,36,39,41,42,44-50,F EE LOG و و‎ mt seem ad 20 e ORLA m NC inneren Barnes (1982) . F ⁊ᷣ ͤ y Se ior AE reve crear At 6,21 Fa (0:9 SUD) EE 39,40 ad ðͤ v ĩͤ E OO LO! Baumgartner, De Wever, and Kocher (1980) ..... 6,10,34,37,42,46 N c rrririserrir" . 5,27, 35, 42, 44, F VI see ee een 11,14 ß y E N ke 11 !!! & 2 · D 3,27, 35,41, F Benecke , voe eee rie ene Hn SERIES TREES eI 47 BETAS IASC neuro EE EUN ER SiGe tt terere 8 e, , . %%% ⁵⁵⁵⁵⁵⁵⁵⁵⁵—— NEAR A ANDAS EE JANE d Naging, ,, is o eare EUS ee AT Beko Banama DN an aa Maka aa ec ar SC Blome (1983) Blome (1984a) Blome (1984b) Blue Mountains island arc complex ... Blue Mountains PANDAAN NG ndi A D S BME MOODS US BOI IL ee: ER oL bona e,, is 1 boneti, Napora .......... qued aan ai TES af ox de 5,27,36,43,F rdf E e Maan IE RET 5,7,14,17,19,20,42 Boreal ett ñ . 10 Boreal Faunal Realm e eee i cde, E 20 Borsa Radiolaria aa y 8 1 Boreal Realm ......... 5,6,8-10,17-20,24,26,28,31-36,38,41,45,46 Northern. Boreal ,, NS TORO 5,8,9,11 Southern Boreal Provinßcdce 5,8,9,11,14,18,19,32 Sower BAUM OVI ON d 2i: Boti COULS ری‎ 8 10,12,33,34,40,46,49,50 NS IS AN e ß 12,13,50 eee, e E ERE 12415 Queen Charlotte Island ......... 7,10,12,20,33,34,40,46,47,49,50 NICO CIOS ee, N er TU 78 daana nb a Gd ß 20 Bio d DD LO CR D NA LR 8 eee NT Ct 6715 5 , re een. 7,8,10,11,17,18,20 CONGCHIUTICANSOWELUN LOLI) er ee 17,50 DU SOS ESOS USES ee S 17,50 Buckman (1892) Buckman (1899) Buckman (1913) Buckman (1918) Buckman (1920) Buckman (1921) Buckman (1922) Buckman (1924) Buckman (1925) Buckman (1926) Buffler, Watkins, Schaub, and Worzel (1980) ....................... 19 eee, e,, EE OF far 27,34,37,42,F eee ee ee eee 49 BIETE e e d ER deal Borc ean E ITON 00 ee 10 PUTER NANG eee, O 5,27,36,37,43,45,F , So oR O 49 EE e 21 rf 8,10, 19,20, 24, 27, 30, 32,37, 49-51 ee MEM 18 ies sas +> ee ee 16 Gan EE ee nee er 49 JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 69 Coast Range ophiolite ..... 8,10,16-19,27,30,32,37,42,46,49,50 Gas RANES nn 7,8,10,16,24,27,30,32,42,46,49,F Ee Deen UE EE 50 // astra 16 ius sun TAE T EH 49 Rane, 8 7, 8, 16, 19,24, 34,49 GROEN ALO ee ,,,, 8 50 Gredt Valley H DEE RE eae S 8,10,17,18 زور۱۳‎ ODSSOHO 49 OSENG OPOE ⁊ᷣ d e r 17 Rene,, 8 8,10, 17 HE An een ea Ee 16,18 VIS TOR Banks see ee EE 6 50 انا نا نز‎ 8 19,20 ITOUCH WES مها‎ HI ee dod dees wR MRNA Ee 17 Ff 8 16-18, 50 ¡BOTAS al een 16-19,30,32,37,46,49 SanaBenito, en,, e HN 16,18 f/ NEK EE 16 en,, y EE 18 MEA 16-18,30,32,37,46,49 agan a اک‎ t lis er E ERR INS 17 eee 8 20 net,, ATMO CER Ae ti vey evince raphe 16 Sale e y 18:19 SODE LOLA a y 18 e,, OUI aa MA ⁊ 16-18 volcanogenic-pelagic strata ........ 8,18,19,27,30,32,37,42,46,49 WESTON IAAT e,, RAN a KN 17 AS ی ای‎ ener مه‎ E 18 i 5, 7,88, 10, 1416, 18, 19,27, 49, 50, F !!!! EE 6,8-11,52 ANA ee ee ی‎ 46 G, d EE 16 anulatum Pessagno and Poisson, 1981 ...................... 49,51,F ens, se 13 tugosum Possagno ANGLE OISSOM TISI ee 49 Gee, E Canutus Pessagno and Whalen, 1982 z Whalen 1982 COLE eS 49 es,, RA ts SINA F SADE EVO SAR cS OR see OE 8,10 GCP NOG OCCEZIG I OR B QUE ora ae eens ose E 20 capsensis, Turanta Pi 49 GardiocerasiNetinayr and Uhlig, HSS e scere e a 11 Canter Crito n GODT URLS SPER EE 12,47 CLON E A N EEE er 1321 CCIE AL TM ChAT SMS AIC ۱۱ casa A 7,13,14 Central Tethyan Province (Tethyan Realm) 5,6,8,9, 11,14,18,19 Central Tethyan Radiolarian Faunas .................... 7,10,17,18,46 et, ͥ d 32-3 cephalopyle 33 e, e RERO RETE dom. S2530 E naja E e C 1 C LEE 49 Cia o ONO ͤ ⁰y ⁰ REAR 14 Cheum رف‎ 7 Sea ß 5210) ELE AO TOLTO NA ee 7 Coast Range ophiolite ........ 8,10,16-19,27,30,32,37,42,46,49,50 Cout ins 7,8,10,16,24,27,30,32,42,46,49,F nee E 49 , d O 47 EE EE E 17,50 eee ! 5 GIG) se NANANG ee NENG rere EE 578 OHO AUS EE E 22:32:33 Gee ,, TU ~ 5,27,35,36,38,39,F GEET 8 27,3, F Gee , nn 11 Crassicollaria intermedia (Durand Delga, 1957) ................... 19 EE E 49 Geiss, RM 5436,20 S o usse c ee SCH e eee See ta Nn di cote ead eee 18,20,32,34 an,, m is 11 e d aAA 54 Damborenea and Mancenido (1979) ... Ss DO) EE EE EE EE EE Decade of North American 1983 Geologic Time Scale .......... 17 EE TEE 50 ee e eff As 8,17 AOS e MA CM een 30 Lv ;( UR I ES 47 DIVE NEM 6223233 T nenne O e 27,39,40,F EE 10-33 39 ASIS ANS IS S SE 27,F Diceratigalea Takemura and Nakaseko, 1982 .......... 22,23,29,30 Dichotomosphincies: Buckman, 1926 x Ene t7 %%% 7,13 Deen ,,,. coe. 12, 14-16, 47,48 dicranocanthus, Acanthocircus discites Standard Zone ... divisum Standard Zone .... TONG e a DNE Darsetensia BUCKIMAN ۱ a ene 48 Douglas (1969) 21 Dine, E 11,30,47,F Pl!!! ß 의의 의 49,F Dumortieria ss... 제 에 sp. cf. D. pusilla Jaworski, 1926 Durand DUET ee, 8 3% - 1149 Lale gerne ah ESO a aa a wer 7 ae e aE a OES GRD SA O elegans, Parvicingula ....... CD aa TUT CTO neueren Emiluvia Foreman, 1973 Enay and Melendez (1984) “Eucyrtidium” ptyctum Riedel and Sanfilippo, 1974 ......... 11,50 Tondmerocenusibuckmanj ne 18 / و‎ iin en corian n ea 50 BANGGT FOENN a a EE 8,20,30 z RA 47 ۱۵۱۱/۵۱ A 8 northwestern western European TIN aa ee 17 رهام(‎ BORIS CO RES oss a ET 50 70 BULLETIN 326 VALLA ALS S crier f NEED Ne 47,48 n, y el 50 dU MIDI ß A ECan 5022.28 26 E SAE se %‏ ور رت e E Zu 5,23,24,25,F J ñr a TM ME ER SN ار‎ gsis 25,۳ SO N d ͤ ̃ ̃ > aso 24 JJ Raum Tr LANES EA So 24 OCU ACT ESI Ne . i SE 24 Fanal Mosaic of the Pacific. Ocean... ae 7 AN O DO UVV. 8 51 FFC K 20 Eischer von Waldheim (i880 is)) RÊ 17,50 CCC) ²˙ AAA... a 6,11 uu EE 48 e aia | ear Reta eye Ah eters EA EE 16,49 Franciscan Complex 7,8,16,18,19,24,34,49 Franciscan melange 7,49 Mais OIRO 11 AO) 시스 이 ys en T pow cete O D es 13,50 REINO NAPONA EXE ee (pb aes. 5,27,39,47,F TUT aire AB) EE NN tq) 8,11,51 r a a 13,20 J 8 Eech I!. 8 8,17 r EE 17 aonana STAC e ͥ³»⁰ÜbQQd ͥ ¹ꝛiÄʃt̃ ee 48,49 V0 AA EBEN ES diss 5,25,26,28,F ۱ OPISDVHUIMDE 2 — 88 48 /// E IS COC RCT ASI VA TIO A ere 11 Ee LEN E a Glochiceras gp. fialar Zone of Cantu Chapa ................. 16,19,51 e 17 ۹۳۱ ۱۱۱۰ OO ee IE 30 JJ! EEE 8 Gorgansium morganense Pessagno and Blome, 1980 ........ 49-51 a E LOOL ی ی‎ IAS 47 CEET و‎ RODE CE OES 9 %%% ⁰ũ ↄ ⁰0 . ᷣ ⁵⁵0dd 49 Ke ah Napora OF sees ZE ‚Al 5,25,38,39, F E Och PODES میا‎ e او‎ E A 13 %%% ⁵p eter eren ANA 2 MS. PON E Sin f ni e d 17 기게 기 Gy ley SEU e 50 re Ve SUDORE TON eee 8,10,17,18 an eg anaa E EC ORS E e Antara Uie A t 8,37,46 LS oig san itu nin Less teen ße ent RAS pod Ard 8,10 e! رد‎ e E OUS een 19 ER Le ee Ne 7,14,19 Haeckel (1881) Haeckel (1887) OA ET 14,15 er y 20 J)) cc MM LR QU CERT NEN 8 13 halseyensis, Rolumbus u... هم مسا‎ les e 5,25,26,28,F P! dE 5,25,26,28,F Harland, Cox, Llewellyn, Pickton, Smith, 해지 er y 17 323333) she OE i Heinen, lee toL 19,51 WEDI NGIDUNGA. ᷣ AAA ĩ 10: 288 5,27,40,F Reim (SD AI E 10 27, 40, F. ۱۰ 8 10,13 Hilarisirex Takemura and Nakaseko, 1982 .... 11,21-23,26,29,30 TS RIN ESD 8 138 1 e , / ater N S 5:2 ODE quadrangularis Takemura and Nakaseko, 1982 ............. 30,31 Hillhouse, Gromme, and Vallier (1982) .... Holcophylloceras Spath, 1927 Fr E HOPO eher es,, re Hopson, Mattinson, and Pessagno (1981) ................... HODSO ! EE re RIE: RUE dë lo Mo 8 6,11 /// V EE E e een, d TIERRA e e e a TTD Dip A AE ای‎ LONG i ار‎ T T EILER A e Hyatt (1900) Ab Fase, ah. 14, 15,23, 24, 26, 29, 34, 41, 43, 47,48 // LR O CRE IA 48 Citi. an ME RE 2l زا‎ OEA NA ONG a erde 49,50 ICZN [International Code Ol Zoological; Nomenclature, 1964] omeia eni tess 23,26 M.... v mM! Re 7 e, REPRE, DU Braune 8 ane, O ET 7. idoceras Burclchardts , i. one ene nee ee 11 Idoceras Zone or Cont Chana oi eT aU RET kea 19,51 r 17 Imlay (1939) Imlay (1940) Imlay (1953) Imlay (1955) Imlay (1961) Imlay (1962a) SN تنل‎ Lang le EE cs ERRORS SEG I /// ᷣͤ T.... OT Lobo Imlay (1964b) .... Imlay (1968) Imlay (1973) Imlay (1975) : Talay (1977 Ka njo , ⁰ʒ | janan کم‎ ak en Imlay (1980, report on referred fossils) ... dina en ACIP SI ea. و‎ N a Imlayzanid en,, D PIRE HON verts NOD OILS ete e Cere recti t eese ee ORE DES DO ayan TIERO ARA R e Iniskinites Imlay, 1975 e ee eee, ²⁵Ü.. x I))... -»' JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 71 z c / era Jet 49 / و ار‎ 5,27,41,42,F (/// emo area 22,32,33,34 coronar IDE WW EVER LOS 25 enter ee 22.932,33 WOOL OSTSEE / re 452 dees 5 E SING SA O EE E E a T I Jacus (?) SEDO e e,), S e . e e ACS area dee) 25,33,34,F S)]!!! IE E ERR UE 25 .. ET EE Sais: 34 sp. B sp. C Jansa, Remane, and Ascoli (1980) Japan Genübdlb ea Warmers, E Mc rs ae remem cra EE 30 Ivano ee d re 30 Jaworski (1926) J. 47 e ae... 6,7,10,36,46,47 WOME SHC OFA cas e EE 17,50 Jongs es Denia ne, ee 7,10 JONES ALU es care d EA f aio eee Juhlei, Stephanoceras (Skirroceras) DUR ASSI Guns LN GN mais MOIS athe ETE OPUS ees 5-8, 10,11, 18,22, 35 e aerate tics Wa caer cvs ²²⁵²mw; 8,10,14,30,F ۱1 ee 5,6,8-11,14,18 LEO WED EE 7,8,14,18,21,23,24,26,28-30,32-34, 38,39,41,43,44,47,49-51,F ING Sa [ah | Aa errereen 5,6,8,10,11,13,14,18,27,30-32, 35-37,39,41,42,44-47,F BBE Ee 5,8,18,19,20,27,30,32,36-40,43,46,49,51,F اک‎ SERRA, A 48-51 TRUS EOD DEE 13 COIN A ga a Peeters cede E AT 13,20 Ken and Gradstens(lO8 Ee eR OR 17,18 Kepplerites Neumayr and Uhlig, 1892 ......................... 11,14,49 1 9 59 9977 8 Je 16-19, 27, 30, 32, 36,37, 43,46, 49-51, F t d O 8,10,17 MONO, ,,, ARS UPR CERDOS 13 d ee 10,11 URSA OAO een lower massive gray limestone member middle thin-bedded black limestone member 13,50 upper thin-bedded black argillite member ................ 13,40,50 Kunga band. BONS COLUM ON er nee 12:13:50 Etat Te e eun ONE S ERN 13 eee eee e 15,47, 48 nes y eke NES 48 !! ᷣ . A N ET 48 E e e 이구 0000 7 e e 1920 << 65 ija ee ee 48 eee e, e 15,47 T aa e aaa an secu XS 11 LEUSSOCETOS ACD , creer cre a Na a TORIS 48 LONESOME kanth na OD ANA KAG NANI HT NIE 16,27,49 ,,,, y 20 / neg eae ren Mere E 7,10,14,19 Wom kayo maka KA OSS NOS TER een D UR NER 7,10,14 lösen Napota: ER ML. ou. 27,34,37,39,42,F IUDICI VER COELI ovem E 14-16,48 Euphersananbaekards COS Opern ció 8 14 , Rs aE E E E 14,48 MacKenzie qo) ß 13 e nud ERU site R 48 Marsaritauus:StandandsZonesr. 22.2... ut 47,49 LEE Mascke (1907) E EE Maude Formation 8 Maude Island, British Columbia .... Mazapilites Zone of Cantu Chapa McWilliams and Howell (1982) EE ee lr EE EE EE Megasphaeroceras rotundum Imlay, 1962b Megasphaeroceras rotundum Zone of Fall and Westenmann (1980). 14,16 Melendez, Sequeiros, and Brochwicz-Lewinski (1984) ........... #7 Don GO Aan ẽ e 13 Mesozoic ieee 8 7, 13, 14, 46 Werra rr haaa ga haaa a 8 NIE a elm C A AN S 7,8,10,14,20,23,36,46,51 Baja California Sur ... 7,8,10,20,23,24,26,28,30,33,34,38,46,51 10800 08 Suadaluiper icc E 20,52 e 38 Ae nee 7, 8, 10, 14, 16, 18, 19,27, 36, 38-40, 43,46, 51 E ELE E EHE. e Kei tto IB VICO EE a) us. o e oet tun e ede E UM Bud COCO Jal A 아사이 A apo add cle tents IG MEISEL ee ی ی‎ ad Tan Vegas 8008 rece ee EST Sy cea MG EE EE EE‏ یا ROT OI Ia ES LT 8 Nuevo Laredo-Mexico (D.F.) Highway f E PROS E a RAM RUSA EE em 비비 ge EE Taman-Tamazunchale area Tampico Veracruz Vizcaino Peninsula: EASES oru ee 8,10,20,24,46,51 TUER HO SE ae ee 20 Mino Deltok Genma Japan: . ES 30 NGISAS دا‎ eae ENA SSS UY, FOURS ای‎ h Sl x. 5,25,26,28,29,F Se , E S S oss 5,25,42,43,F // nennen W 기 5,27,43,F mociezumaensis GE), NGDOTA. issa 9 27,43, F Monotis : HOCUS GABBA Od... ی ما‎ asd nen کف مه مور‎ 13 speck Mosmbcircularis Gabb, ß ne 13 f.. (Dm ß 49-51 ( e UNS 5,25,43,44,F Oh DUIS een en ↄV F TV Guter S E EE E 50 Nee دی‎ E 14 rr 47 . / de eee ter eT 50 e m 17 el,, EE EE 8 Napora Pessagno, 1977a .... 11,21,22,32,33,34,37,38,40,42,44,45 UHCIODEHSIS, r 8,111 5, 27,34, 45, F baumgartneri, n. sp. ............ dr ecu 5,27,35,42,44,F EE SR poe 5,27,35,41,F DO OS LE RL S ales EE 3,21,308 GCP 8 N 5,27, 36, 43, F C ⁵¼:—— ERR Ee ee 645 5727,35,36,3 7; F bukryi Pessagno, 1977a geni. 27,34,37,42,F NTC 10 2: 5,27, 36, 57, 43,45, F CETVOMICSACTISUS TAN SD Sees dacs IU TECH 4 5,255960, E CI! / و7211‎ 5,27, 35, 36,38, 39, F , ß O ance. sees 6737 27,39,F deweveri Baumgartner, 1980b sensu lato ........ 10 275 40, F sp. aff. N. deweveri Baumgartner, 1980b ............. 10 39 Sp. cl. N. dewever? Baumgartner, 80 , 이 27. Jructuosa, DI Spe ent 5,27,39,47,F heimi, xo spi eie eee 5,27,40,F sp. ENE TODAS WE SD ciem همه و‎ hne 10: ~ 27,40,F V; A ee 6 5,27, 40, 41, 46, F insolita; m 90. scar su 5,25,41,43,F 7770 Sls ra 5,27,41,42,F lospensisPessagno; a 9 woes 27,34,37,39,42,F R ĩ TT Tb nec 5,27,42,44,F 6d. A UNUM S 5,25, 42, 43, F ee r tine ses 9- 5,27,43,F sp. aff. N. moctezumaensis, n. p 99 27,43, F CTV kennst Sera, 5,25,43,44,F SANE 대 비즈 in ee 6 55 5,27,44,F ee een 88 spinifera Pessagno, 1977b ......... Renn spe 2 3323 edes JV0VC0VV%%%% sp. sp. sp. sp. sp. sp. sp. sp. sp. Napora (?) graybayensis, n. sp. ............. DPA A 5,25,38,39,F eee r ͤ 19,51,52 Neutra Rand ene, ERE pn 11 Fenner and Uhlig (1892). cassette e 11,14,49 Nicely Formation .... 14,15,23,24,26,28,29,34,38,41,44,47,49,50 nitidum, Perispyridium 49,F CP!!! ðr OS REDE OE ee 49 EE EE 10,13,20 Normannites Munier-Chalmas, 1 892222ü : . 11 Norii ae: 1 101 22 Cordilleran Region ۱ ۱۱ adeo E E EE i 10 Nor ieee... 8,10 Norii Slope, d 8 8,10 BULLETIN 326 Nonnen Boreal Assemblage ee 10 Northern Boreal Province (Boreal Realm) hp) 5,8, 9,11 Northern end.... iced tines en 8,10,12,16 Nexthern-ketihyanıBaunal eee 27 Northern Tethyan Province (Tethyan Realm) ... 5,6,8,9,11,14,18 Northern Tethyan radiolarian faunas ................... . 10 OMMELENSISALUPANIIQS nt AR NOR 8 48 Gil. Ma 8,10,19 / / DE 5,27,44,F Opalintimn-Standands Zonen tates N 15 Oppel@l896-1898 ster isi net eot ie OU YEN 51 d'Orbigny (1844) e IRRE 50 Ges) Iu UE 1281 ele k 88 34 Bear Valley Sr Bear UE Fanger ass 8 48 Blue Mountains island arc comple Ass میم‎ 14 Bine Mountains ee, 5,7,8,10,13,14 Büffet, 8 Bunton Hollow BUESA ی‎ ida arvana ee (any ott Gilby OCA eH vaa EE و‎ eee Caps ee... „ Central melange terrane GIOOK e,, teet rs Duncan Hollow 47,48 CAS e,, E 6-8,10,12,13,20,23,24,26-32, 34-39,41-47,49,50,F ell 8 Elkhorn Creek m Bl @IOCK i pin A E ee Grant County Graylock Butte 24 راما و‎ DAS a SENDEN E arias 12 Harney County 12 , EOS nias vs eee e etae ea tee RN 47 PON atO VETADO un ivre avi E Cress 7,13,14 EJ“ ( REE 12,15, 16,41, 47-49 ee Faid, een 47-49 JD A reve tin en: . 6,7,10,36,46,47 TORE IO KANO a ee ene 12,16,47,49 South Fork 12,16,47,49 e ad ARA 48 Lewis as EEN 48 Ee Sows hot ee. 8 48 Mesozoic clastic terrane 7,13,14,46 Morgan’ enn 43,47 northeastern POR naga sh everest eve EARAN EE 15,16 Rosebud? GUION nn 8 16 Rogue Valey subterrane wo veces Ee 17 Shoo Monee PMO ereraa 15,47,48 Seven Devils terasse 7,13, 14 BAWANI eee 8 48,49 EE ROIS OAS E CR 49 Silver Creek 12 Si Vies SG id=) an en “ 12 Sabe IS Ver isse wein aan ehe 2 90 sss, 8 48 BOLNE SVETI 8 17 SO E OVE o una 12 JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH 73 SUPC ZES ale Apos seen votes Wallowa Mountains J ars Er CR AN IU. FTT S SAE SOTA 5. EE EE 10,14,17-19,50,F Pachyonchus Pessagno and Blome, 1980 .......... 49 ,,, esaa 49 Pacific Ocean CASUCLIM Hv uc E ee ß y Pacific Rim Complex ...... packardi, Perispyridium TRATA TE Dellandres OSB ee 30 Ee E EE E Palmer (1983) pantanelliids (ROMANUM POSSANO LOT 11 DauleyaBessapngrandıBlome LISON sccm cease 48 Kinense Pessagnorand Blomec| , e 13 malheurense Pessagno and Blome, 1980 ........................... 48 EE 20 VA RANA rest AN MN 0 o ese 49 VINE AAA 19240 et LEES 10 ON Se e a a eng el 6 Parvicineula RessdenO; 197 TA e S 5,8-12,14,16,18,19 blackhornensis Pessagno and Whalen, 1982 ...................... 49 burnsensis Pessagno and Whalen, 1982 … … … 49 elegans Pessagno and Whalen, 1982 ........ 49 grantensis Pessagno and Whalen, 1982 .......... 49 matura Pessagno and Whalen, 1982 .............. 355 ß eerie cee 49 profunda Pessagno and Whalen, 1982 16 Santaba ra EE ,, 16,F schoolhousensis Pessagno and Whalen, 1982 ..................... 49 verasBessaeno and W UALS, OR Qe... eects) eevee cee 16,49 EE 16,19,47 e eee Na na ei ce ie dde 16,17,19,49,51,F ¡DARVIN S TGCCONOCUIVOINING e ITO 47,49,F KEKOS SVU eee, e,, Ty 48 Perispyridium Dumitrica, 1978 ................ dumitricai Pessagno and Blome, 1982 e, foremanae Pessagno and Blome, 1982 ... gemmatum Pessagno and Blome, 1982 ..... Se UUM Possagno and BIOME, 1982 Ee Packardi POSSE MO AIG BIOS SEU SS TN e cc se ae 49 tamarackense Pessagno and Blome, 1982 ..................... 47,48 eee a eel lac dl 30 ES EQ e T UO 21 Fd 20 a aes ee ices 5,6,8,10-12,14,16-22,32,34, 37,39,42,47,51,F FF 5,6, 19-22, 24, 26, 30, 3234, F eff de UO SE EE 16 Possagno (VOP ANSNI AMA) anan nea a 10 Pessagno and Blome (1980) .................. 6,10-16,19-21,47-51,F So and BIOME (L982) NE ee 6,11,16,47-49,F Pessagno and Blome, ,,,, era 7,8,10,14 Pessagno, Blome, Carter, MacLeod, WHALEN, ABC KORD Dres) aaa saga as en NT NM 6 Pessagno, Blome, and Longoria (1984) ........ 6-8, 10, 1621,32, 37, 40, 43, 46, 49-52, F Pessapno, Finch and bee, eee 20 Pessagno, Longoria, MacLeod, and Six (in press) ... 8, 10, 19,20, 52 Pessagno and MacLeod (unpublished data . 47 EE ما )ان ودره‎ ris 6,47,49,51,F Pessagno and Whalen (1982) ....... 5,6,8,10-16,18-19,21,47-50,F ایس واه ان ای ناه تست و‎ OE ی‎ REESE Sa 8,19,52 eee ,,,, 14 eee and Packard; T930 uere 14 Rensen ttt 10, 13-15, 20,21, 23-26, 28,29, 3234, 38,41, 44,47, 49-51, F PodocapsaamphürepteraKoreman, d 8 11 Praeconocaryomma parvimamma Pessagno and Boissons 188!!! 47,49,F e yd Ee 48 DIVO DUNE NOONE CGS Se ARE en aaa 33 DIO gens ½½//////// h ee 51 PRO OUS ROT ß, y UE Ios 16 Rroniceras: Burckhardt, d ? 8 10 protistans 11 Peendocadoceras- Buckman ͤ 8: RA 14 DU GI TES TIM, ES S ee 11,50 ELE , d said RENE 8,10 PUSIMOS ORE AUN. bn A LE. apre nee 47 DUSQLQNGE)SID EE 47 Quadra Suar iS Iam qe a APT 이시이 30,31 Queen Charlotte Islands, British Columbia ...... 7,10,12,20,24,33, 34,40,46,47,49,50 (00% ᷣ mmm csset E 39 P ð wd ee E 12,13,30 eur Leg cede u m 12,50 ]]) RR 12:33 Sasse ile. 8 12,50 ۵0 و‎ (iS 8) ne ی‎ y 49 Taricosiatum. standard Zone ann... A eee E 50 Led BH DOOR CBOSS ne cem 7,10,16,18,19,49 ; 8 ASS: d 5,25,32,33,34,F // a OS 11,14 Fes 8 30 PUNJEN f 21 RiedeltandiSantilippo (19 EE 121550 Ristola Pessagno and Whalen, 1982 5,8,9,11,18 AMA اد‎ A F sp: Aff R deco Pessagno and Whalen, 1982222 50 hsui(Bessapho f,, OSB Se E F Ristola (?) turpicula Pessagno and Whalen, 1982 .................. 49 ENEE 5,21-23,26 Ff!!! ee 4 2 5,25,26,28,F d 3 50M 5,25,26,28,F hamiltoni, n. sp. ...... Sc? DAS 5,25,26,28,F TTV ey ae 5,25,26,28,29,F VERUSTUS E a SP) E becca cens KANG en alte S Ix 5,25,29,F SD iO hes tig M dn d m s 253E ene, EE 17 ,,, deve ciae BA TUE 48 C 8 14, 16, 48,49 ee eee meee rake 17 r d sues 17 OUST OAS ae 7,8,10,11,17,18,20 56k) AA AA EE 17,50 e / EE 49 74 BULLETIN 326 Tonne ار‎ T REA KN Kak KA TU a AA gen s Make , ß A A 11,19,50 10 es mshi CT OI LO h cio ee 8,10,11 Rüst (1885) ... , ß 11 Rüst (1898) ... r Pen ned cro ERENTO 48 r // awe 15,16, 48,49 !...! kde e ER 17 Tee E ARS h..., an 17 Saleeby; Harper; Suoke; and Sharp ی‎ eee 7 Subneumayria profulgens (Burckhardt, 1906) ....................... 51 S ,, HR ARE s 52 Suplee Formation 14 San Hipólito Formation.. 20,23,24,26,28,33,34,38,51 Sutherland Brow (1 y 13,50 eee, EI Ren 20 Sutkerland-Brown هه‎ ssa E %% ana 20 n esera a 17 POSED رو‎ Eege AR 20 sandstone member 20,23,24,26,28,33,34,38,51 /// DR 5,2933, E Takemura and Nakaseko (1982) ...... 5,6,11,21-24,26,27,29-31,F sandspitensis (aff.), Jacus (2) n. Sa, 25,33,34,F Taman Formation .......... 8,10,16,19,20,27,36,38-40,43,46,51,52 SUntabarDaraensis, Parvieingulge. SE 16,F lower more massively-bedded unit .......................... 19,51,52 SE r nn ne 19,52 SEER ness... ee , , ĩé].0 ae 47,48 Scaled Equal Subzone Method of Westermann, 1984. 18 Taylor, Callomon, Hall, Smith, Tipper, Scarburgiceras Buckman, 1924 11 and Westermann (1984) ne ee: 7,8,10,14 schilli Standard Subzeennne 17 Ad RR T EN E 16 schoolhousensis, Parvicingula 49 lll 8 SOS, es,, دی‎ x 47 e na ana kona ia ays 0099899 ed ae Seo DN ea npe rs PR NT a 9 Tetbyanskammal Realm ren... EE „„ PVC RE H Tethyan Pantanelliid Assemblages Seven Devils terrane Tethyan Radiolarian Assemblage Siemiradzki (1898) ......... TeihyamRealmiwern 8 5,6,8,9,10,19,24,26,28,29,31-46 Sierra Madre Oriental Central Methivane Province oreren wheter 5,6,8,9,11,14,18,19 a a A ASA ðx ĩð eee INS Norther Lethyan Provine ne 5,6,8,9,11,14,18,19 JC O a AA A O T 48 ,, ne, silviesensis, Turanta Southern Tethyan Province „2 O KA مس‎ E EE 0 .“ a 48 e , y Ge E OR DU E N SEE RE 20 AE en SE Smith, Hurley, and Bridan (1981) 8,9 Dapper 98er... , een eek 6,14-16,47,4 tipperi, Canutus e nee 47 PR CIO Se nee TER Sun River S0bleraner ann re 17 nee s,, Bu 2 paleoequator Snowshoe Formation. 8,14,15,23,24,26,27,29-32,35-37, eee ee SOD EE ۱19 39,41,42,44-49 A ,,, ʒ E 47 CCCC%%%%% LIN TON 15 c ee 8,10,12-15,21,23,24,26,29,30,32, SEBO OSE Member. ee tee 15,16,48 34,41,43,47,49-51,F F A A EE 15 ee ETC ET DU C EE 14,49 South Fork Member 15,16,31,35,39,42,45,48,49 i , r Warm Springs Membern 14, 15,23, 26,29, 31,32, 35-37, En ENEE 39,41,42,44—49 Ie E Fere Ur gr Me ya SOON dere Formation eo qoc ⁊æqꝶq ES 49 NG Pe ter cr cr EE 2222! e C, bas ono BEA 11,47 Trillus Pessagno and Blome, 1980 00% EE 48 elkhornensis Pessagno and Blome, 1980 ................... 49-51,F J%%%%0% S me T tes در وی‎ ( 48 /// 11, F f oo a eet ie E RE Rd 8,10,16,46 Tropidoceras actaeon (d'Orbigny, 1844) E(E( . 50 Southern Boreal Assemblage 10,18 /// . 13 , 0. 2 27 BLOM TICES Yo tana a Bi nan ea eos A 15,16,48,49 Southern Boreal Province (Boreal Realm) ... 5,8,9,11,14,18,19,32 Cf!!! CURAR dae ERIS 9 5,27, 44, 45, F Southern Boreal Radiolarian Faunasss . 10,17,19 e,, 11. F. ß eis... RE HERE 11 barbara Pessagno and Blome, 1982 sees 47,48,F f trt rere eris HA ERR DAE N WIE S0, /// 49 Spath (1923) morinae Pessagno and Blome, 1982 . F Spath (1928) nodosa AO BIOMOL kaa ana scares cnet 49 ai,! EE EE 11 Oe esI Pessagno and Blome; IG 48 spinatum Standard Zone .... 47 silviesensis Pessagno and Blome, 19822 N. 49 SOD CHAIN ADOT Aree anne air an ĩ مه وم‎ foes 33 ,,,, ORT ROLE 5,27,45,F Spiroceras bifurcatum (Quenstedt, 18588) 49 DIA EE URN LM 8,10,49 ۱ | | | | | | | JURASSIC NASSELLARIINA: PESSAGNO, WHALEN, AND YEH TS تن ی‎ eee EN 이구 E ONE UU PA ne a eT 20 Virgatosphinctes mexicanus-Aulacomyella neogeae Zone of turpicula, Ristola (?) 49 CANO riso E d PA AM 16,19,20,51,52 Vizcaino Peninsula, Baja California Sur ........... 8,10,20,24,46,51 URIE ISOT e ee 8 10,11 Ultranaporidae Pessagno, 1977b ........... 5,6,21,22,24,27,30,32,F is ee Wallowa Mountains die Ultranapora Pessagno, 1977b ; i : 1 ASEO c e en ee University of Texas at Austin ; Westermann (1981) Ummoni BUCKMAN ß y y ebro ; ; Westermann (1984) Spach U. duyiceroides Monterde; 1984 ees eerie ne 50 à 1 1 ß nn 16 USGS [United States Geological Survey] : ۱ Westermann and Riccardi (1979) ee Va DEH Vere QUE e UH C ATE A ga a Sens 20 i /// d ele aT ers een ne nee lee een 50 ۲ i z!!! O A Mesozoic locality W O Pen Ta NEST: 47 = ER EE ee EE 48 EE EE 2% EE 49 : 3 4 DOE e ee RE 48 c serie 9 ره‎ Me e 8 48 : Nu x e vy A EUM 48 ,,, ß ی وی‎ AA 13 Wan ß 8 SUI ۲ ene, 11 USNM [U. S. National Museum of Natural History] — وس‎ ee 21.24. 26.28 29,31.33.35-46 PA Possagno and Blome, 8 48,F JJ) ¼ a Se: C jonesi Pessagno.and Blome T980 ceases AD Jurassicus Possagno and Blome, 1980 ی‎ ne 48-51 NAMES تن‎ NEE 20 praejonesi Possagno and Blome, , ca ass 48 Vallupus hopsoni Pessagno and Blome, 1984 U•—ͤU UA F thayeri Bessagho and Blome, 1980 east 48 Vancouver lslandsbuush@olumbare u 7,8 Zone | of Pessagno, Blome, and Longoria 17-19,50,51 VOISINS f E A 50 Zone 2 of Pessagno, Blome, and Longoria ......... 16-19,32,36,37, PANAH Standard Zone e RI EO 15,47 42,43,46,49-51 6»! 8 OT NA 527.458 BONS ku simil A een ee 48 V Usama ان‎ TREE 8 5,25, 29, F Zone 3 of Pessagno, Blome, and Longoria ......... 18,19,37,39,40, 0 uo ic Ga ee ee dE 16,49 42,46,49,51,52 Natiassa f, 6 Zone 4 of Pessagno, Blome, and Longoria 18,19,46,52 Text-figure 7.—Range zones of Lower, Middle, and Upper Ju- rassic species assignable to Farcidae Pessagno, Whalen, and Yeh, n. fam., Ultranaporidae Pessagno, 1977b, and Hilarisiregidae Take- mura and Nakaseko, 1982. L = Lower; M = Middle; and U = Upper. Numbered biohorizons (broken vertical lines) used for biostrati- graphic and chronostratigraphic reference (see below). LOWER JURASSIC MIDDLE JURASSIC UPPER JURASSIC — Canutus Pessagno and Whalen, 1982. 2. Canutus tipperi Pessagno and Whalen, 1982. NO ۳ 6 3. Canoptum anulatum Pessagno and Poisson, 1981. The bioho- INFORMAL SUBDIVISION L L O L ~ 세 Ｌ 3 L L U rizon defined by the first occurrence of C. anulatum may occur a in the upper part of lower Pliensbachian (see discussion in Ap- NUMBERED CCC 7 9 ۱ pendix: California Coast Ranges; Lower Jurassic 1065. NSF-958, BIOHORIZON — No megafossil control NSF-959, NSF-960). REFERENCES P Last Occurrence 8 e pos 4. Trillus elkhornensis Pessagno and Blome, 1980. 5. Turanta Pessagno and Blome, 1982. Napora (?) graybayensis, n. sp. 6. Praeconocaryomma parvimamma Pessagno and Poisson, 1981. ee 에 주 7. Perispyridium Dumitrica, 1978 (see discussion in Appendix: east- Noa an central Oregon; Middle Jurassic loc. OR-593). = A i š A Jacus sp. id 8. Turanta morinae Pessagno and Blome, 1982 (see discussion in 7 ues : 4 Appendix: east-central Oregon; Middle Jurassic loc. OR-580). arcus gray'octensis, n. Sp. - > ; 9. Turanta barbara Pessagno and Blome, 1982 (see discussion in Jacusi Uisp ad T A ganda E S — | Appendix: east-central Oregon; Middle Jurassic loc. OR-555). F سسسسسه‎ 10. Zartus imlayi Pessagno and Blome, 1980 (see discussion in ی(‎ SP. e t€ Appendix: east-central Oregon; Middle Jurassic loc. OR-513). Rolumbus hamiltoni, n. sp. — 11. Perispyridium dumitricai Pessagno and Blome, 1982. Rolumbus venustus, n. sp. — 12. Tripocyclia Haeckel, 1881 (see Pessagno, 1977a). This taxon is Rolumbus sp. important because it occurs both in the Tethyan and Boreal Farcus asperoensis, n. sp. SE Realms. Rolumbus gastili, n. sp. a D 13. Perispyridium nitidum Pessagno and Blome, 1982. Rolumbus halseyensis, n. sp. prana nanak D 14. Parvicingula Pessagno (1977a) sensu stricto. Parvicingula s. s. Jacus reiferensis, n. sp. تسه‎ 2 includes forms like P. santabarbaraensis Pessagno, 1977a, which Napora cerromesaensis, n. sp. "eege possess a long, slender tube on the final post-abdominal cham- Rolumbus mirus, n. sp. punc ber. Napora insolita, n. sp. E و‎ 15. Ristola hsui (Pessagno, 19772). Napora mitrata, n. sp. — 16. Vallupus hopsoni Pessagno and Blome in Pessagno, Blome, and Longoria, 1984. 17. Ristola altissima (Rüst, 1885). Napora fructuosa, n. sp. Hilarisirex sp. Napora bona, n. sp. Napora browni, n. sp. Napora sp. aff. N. cosmica, n. sp. Napora turgida, n. sp. Napora opaca, n. sp. d Napora baumgartneri, n. sp. sme 2 = = Napora horrida, n. sp. Napora maritima, n. sp. Napora cosmica, n. sp. = Napora bearensis, n. sp. sen Napora antelopensis, n. sp. Napora izeensis, n. sp. Napora tumultuosa, n. sp. Hilarisirex oregonensis, n. sp. Hilarisirex inflatus, n. sp. Napora moctezumaensis, n. sp. p= Napora sp. aff. N. moctezumaensis, n. sp. 7? — 272 — Napora vegaensis, n. sp. Napora boneti, n. sp. Napora bukryi, Pessagno Napora lospensis, Pessagno AI UL d Napora sp. cf. N. deweveri, Baumgartner Napora burckhardti, n. sp. Napora deweveri, Baumgartner Napora heimi, n. sp. Napora sp. aff. N. heimi, n. sp. = —X xj Kg Kë en, amete PREPARATION OF MANUSCRIPTS Bulletins of American Paleontology usually comprises two or more sep- arate monographs in two volumes each year. This series is a publication outlet for significant longer paleontological monographs for which high quality photo- graphic illustrations and the large quarto format are a requisite. Manuscripts submitted for publication in this monograph series must be typewritten, and double-spaced throughout (including direct quotations and ref- erences). All manuscripts should contain a table of contents, lists of text-figures and (or) tables, and a short, informative abstract that includes names of all new taxa. Format should follow that of recent numbers in the series. 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Size of lettering for text-figures. Journal of Paleontology, vol. 36, p. 1402. Gilbert Dennison Harris (1864-1952) ° Founder of the Bulletins of American Paleontology (1895) ISBN 0-87710-406-9