2. t J ec eGR RS ey ARs * AR Re ee 2 iota astatehts q ee 4 2 8-8 . nS A eta ae athe AAS un OC rr te he r cae mae *. i) qale a aren gata eee ‘. nei YS 4 Waar atahesiee we 4 Rado a eat EAU ea o0| Seah. *_ Pea ceraremesegs oa Fab Wom et ' evi Dear Pg Oe Ch Phe d| f ee ¥ < 4 Eee) aiae Res Se : Pel CRYPTOGAMIC PLANTS OF THE USSR Volume VIl Z.1.GLEZER SILICOFLAGELLATOPHYCEAE TRANSLATED FROM RUSSIAN Published for the National Science Foundation, Washington, D.C. by the Israel Program for Scienti ific Translations 1) *> f Mea A , ar tT yi AKADEMIYA NAUK SSSR. BOTANICHESKII INSTITUT IM. V.A. KOMAROVA Academy of Sciences of the USSR. Komarov Institute of Botany CRYPTOGAMIC PLANTS OF THE>:@.S8.S5.R. (Flora sporovykh rastenii SSSR) Volume VII Z. I. Glezer SILICOFLAGELLATOPHYCEAE (Kremnevye zhgutikovye vodorosli (silikoflagellaty)) Edited by M.M. Gollerbakh Izdatel'stvo "Nauka" Moskva —Leningrad 1966 Translated from Russian Israel Program for Scientific Translations Jerusalem 1970 -R8 Cr a 2 f TT 70- 50046 V. fi Published Pursuant to an Agreement with THE NATIONAL SCIENCE FOUNDATION, WASHINGTON, D.C. Copyright © 1970 Israel Program for Scientific Translations Ltd. IPST Cat. No 5698 Translated by A. Mercado Edited by B. Golek Printed in Jerusalem by Keter Press Binding: Wiener Bindery Ltd., Jerusalem Available from the U.S. DEPARTMENT OF COMMERCE Clearinghouse for Federal Scientific and Technical Information Springfield, Va.22151 VII/7/3 Table of Contents AeA TUCO arse) cece cvetat cus age don Pom wer Pier. s: Land rome babel goon adie ytes Macey ca suxanes, Tides I, GENERAL PART 1. History of studies of silicoflagellates .. -- ee eee eee ee ee eee General characteristics of silicoflagellates ....... 5022-2 eee MESUDHOID OV Sos sa se ees Mone eh eR SP oe ee ot ee ef OO GUCITO cus, as Gast es Ee oe awe wk same A Seem eee BC RIPV icicle ein %) oe nis Piers FEE RES Bade Bee eset Betgr eke 3. Introduction to the systematics of silicoflagellates ......+..+.-.- Position of silicoflagellates among the algae... 1... 5-2 eee . Principles of classification of silicoflagellates .......+2226-- Classification of silicoflagellates .. 2... 2s eee eee eee reese 4, Distribution of ancient silicoflagellates on the territory of the USSR European [western] part of the USSR .. 2... 2.2.22 eee eer eeees Caucasus, western part of northern Caucasus... ++ +e ee eee eee Eastern slope of the Urals and West Siberian plain ......4.-++-2--s Central: Asia, -Aral=Gaspian, area) ae. shor eine e SH ANS ee oe lal Gs PAM EASE. TG OR GR is. eM SU ee ee tee! tos TS care ee SP te Ee 5. Evolution of silicoflagellate flora . 2... 2.520 swe eee ee eee Silicoflagellates of the Mesozoic ... 2... 2.22 ee eee eee ceee Silicoflagellates of the Cenozoic .......++--s Poet 3S elias ies maces 6. Phylogeny of silicoflagellates .... +--+ +e eee eee i sh a ats Ml, SYSTEMATIC PART Class Silicoflagellatophyceae Borgert .. 1... ee eee eee ee ee eeee Order Vallacestales Gleser APs ete ee ff ole 58 ele Pamily Valiacertaceae Detl oe a seh sk ate tea ss ee Se > Gea 2. Variaceriea Tanga es 2 ies = 2s 6 9 Wo 8 8 ws Order sipponotestales Lem. ws es 6 pe ew ns 8 6s ms ee Family Cornuaceae Gem. . 1... 2-2-2 eee eee eee eee ees Genus 2. Lyramula Hanna .......2.--+.-:% Sina’ einen Gente dior MWA rSeMUls Core. i. Dehn whe wilt ole leis oie iil Family Dictyochaceae Lemm. ...26eseeeeceecenseves 240 Getus-4,: Di ety Gelra irs 8. Wa ie tetas sek. os me ois 241 Gents S.C orbisenra Hantia’'s. 2754s. S25 ow le alae aoe 270 Genus 6. Naviculopsis Freng.. soa «-> 5 «sy haneye, eae ate 272 Genes." Distephares Steer wie os js on nh ep eee 278 GCenpe 3. Ratedictyochs. Frese, so 46 ao ates 2 ae 296 Genus'S, Cannepilus Hack. 05 0d cs oe + o's eee Se 299 Genus 10, Meese ce ma Pits. els) 2, a ace wwe es tec 302 RE hae eo en Sew ee en ee Ge oe oe ae a 308 BRT AD (oo a ee a oP ik ne Ce eal sek bee a ee eS ae o. «| ee Aipuabetical index.of Latin Napies..< sa wis ces 2s sv oe ew & 2 ee 358 lamt of Abie Vidette” Sores al pense dae ee gee Aca: Aly = al See be ee 362 5 INTRODUCTION Silicoflagellates are a small, but very unique group of algae consisting of a total of 12 genera and about 50 species belonging to 2 families. Most of the species are extinct; there are only 5 species and their varieties, belonging to 3 genera and 1 family, living in present-day seas. Taxonomy of silicoflagellates is based largely on the more abundant fossil material. The limits and relationships of the different taxons can only be determined by a study of both living and extinct silicoflagellates. Therefore, the major works on silicoflagellates, such as that of Gemeinhardt (1930) published in Rabenhort's ''Kryptogamen-Flora,'' deal not only with living forms, but also with all the known fossil silicoflagellates. The monographs by Schulz (1928) and Gemeinhardt (1930) are somewhat outdated, while the work of Deflandre (1950) cannot be used as a key since it covers only a limited number of forms. Reviews of silicoflagellates have not been published in the USSR; indeed, on the whole, there are very few special works on the group. The use of lists and other data from publica- tions is often difficult since diagnoses of some species and even genera differ from one author to another. Moreover, only a few taxons have been described in the Russian language. Because of this, the present review is based not only on a critical comparison of publications, but also largely on our own studies. Microscopic examinations were made of about 550 specimens from the Upper Cretaceous and Quaternary rocks of the Leningrad Region, Belorussia, the Ukraine, the Middle Volga area, Northern Caucasus, the eastern slope of the Urals, the West Siberian plain, the Turgai Gate, the northern Aral area, Kamchatka, Sakhalin and the Kuriles. In order to clarify the distribution of various forms specimens were examined from Denmark, Hungary, New Zealand, as well as samples of living marine plankton. Part of the material was obtained during field work carried out in 1956 — 1957 inseveral areas of the Sverdlovsk Region (as part of the northern group of the West Siberian Expedition of VSEGEI). The descriptions of core samples and selection of material were made after consultation with the geologist V.S. Pevzner. In addition, I analyzed specimens collected by F. A. Alyavdin, A.G. Ber, V.A.Grossgeim, A.P. Zhuze, M.N.Klyushnikov, O.S.Korotkevich, P. F. Li, R. Kh. Lipman, B. M. Mikhailov, D. V. Osadchei, T.I. Osyko, V.S.Pevzner, L.S. Teplova, I. A. Khokhlova, V.I. Yarkin, M. V. Yartseva and others, as wellasa collection of Far-Eastern Neogene specimens sent to me by V.S. Sheshukova-Poretskaya. I wish to express my sincere gratitude to all these persons. Finally, I also analyzed preparations from the dried collections of the MGU, from P. T. Cleve, I. D. Moller and H. Baecker, from the teaching collection of the Department of Lower Plants at LGU, and from the collection of the Paleobotanical Laboratory of VSEGEI. In most cases, the material examined is associated with specific geological sections. The text includes descriptions of only those outcrops and deep wells in which silicoflagellates were found. These descriptions (abridged) are based on material from geologists to whom the respective collections belong. The established complexes of silicoflagellates were dated mainly by use of both stratigraphical and paleontological data. Accordingly, the chapter on ''Distribution of Ancient Silicoflagellates on the Territory of the USSR" covers major publications on the stratigraphy of the given areas. In all the samples from the eastern slope of the Urals and the West Siberian plain, as well as in some samples from other areas (except the Far East), diatoms were determined to verify dating of the complexes. With respect to this, it was necessary to include pertinent Russian and foreign literature on fossil diatoms. The technical analysis of specimens was carried out as described in the work on diatom analysis (Krishtofovich, Vol. 1, 1949). After boiling the rock in a 5% alkali solution, small mineral particles are removed by decanting a 12-cm column of water from the beaker every 1.5 hours. This operation is repeated until the liquid is completely clear. Silico- flagellate skeletons are removed from the precipitate by the addition of heavy liquids (PD-2, PD-3, and PD-6) whose specific weight is 2.63—2.65. For slide preparations, a special balsam with refraction coefficient of 1.67 was used. The silicoflagellates were examined with an oil immersion objective at a magnification of about 1,000. Forms were counted with an oil immersion objective (60 X) at a magnification of 450, andin several cases with an oil immersion objective (90 X) at a magnification of up to 1,000. Numbers were estimated visually according to a 6-point scale described in the first volume of ''Diatom Analysis" (Krishtofovich, 1949). The following arbitrary quantitative grading of silicoflagellates is used in this work: .— very rare (1—5 specimens per preparation); — rare (10—15); frequent (25— 30); — common (1 specimen in each row of the slide); — abundant (several specimens in each row of the slide under oil immersion objective); very abundant (several specimens per field at the same magnification). or WD Fe | op) | The chapter on "History of Studies of Silicoflagellates" deals briefly with the main trends in the study of this algal group. The chapter "General Characteristics of Silicoflagellates" is based largely on published data. The chapter "Introduction to the Systematics of Silicoflagellates" analyzes the position of silicoflagellates and discusses various taxonomic principles. Under "Distribution of Ancient Silicoflagellates on the Territory of the USSR," there is a brief outline of the stratigraphic position and age of the rocks examined within each area with descriptions of the sections, the major diatom complexes used for dating the different deposits, and comprehensive lists of the silicoflagellates encountered. 7 In the chapter ''Evolution of Silicoflagellate Flora,'' the material is reviewed according to geological periods; a review of the literature on the respective floras and my own pertinent observations are included in this chapter. The main features of the complexes of silicoflagellates of the different areas as a function of time are discussed here. The chapter "Phylogeny of Silicoflagellates'' is based on material given in the two preceding chapters and contains a critical evaluation of publications. In the systematic part, each form is accompanied by its synonymy, original description, paleontological or taxonomical features, as well as past and present distribution. For determination of the silicoflagellate species keys are given in the systematic part. The magnification of the original drawings given in Plates I— XXX is 800 times. After the manuscript was completed, some new publications in the field came to my attention (Stradner, 1961; Bachman and Ichikawa, W9/62% Bachmann, Papp and Stradner, 1963; Tsumura, 1963; Jerkovié, 1965). These works could not be included in the systematic part, but the new material enabled me to determine the stratigraphic position and age of some of the complexes whose properties were previously unknown. For example, the complex provisionally dated as Early Oligocene and placed inthe Kharkov (?) suite, which is widespread on the territory of the Ukrainian SSR, turned out to be part of the upper zone of the Kiev suite since it dates from the end of the Late Eocene. The complexes established for the Chegan suite on the eastern slope of the Urals and in the West Siberian plain and dated in the Late Eocene— Early Oligocene (?) and Early Oligocene (?) are actually associated with the upper part of the Irbit suite and the upper part of the upper Lyulimvor* subsuite, respectively; these suites date from the first half of the Late Eocene, and the silicoflagellate complex associated here with the Early Oligocene (?) apparently belongs to the very end of the first half of the Late Eocene. All these data could not be incorporated into the text. I wish to express my deep gratitude to V.S. Poretskaya, Senior Assistant in the Department of Lower Plants at LGU for permission to use their collections and valuable special literature, as well as for advice and constant interest in my work. I am also indebted to Professor I. A. Kiselev for his valuable advice. Finally, sincere thanks are due to Professor I. M. Pokrovskaya, head of the Palynological Laboratory at VSEGEI, where the work was carried out, for constant support and assistance. * [Also given in some references and in the original text as Lyulinvor. ] ABBREVIATIONS OF NAMES OF REGIONS OF THE "FLORA OF THE USSR" USED IN DESIGNATING THE DISTRIBUTION OF SPECIES European [western] part of the USSR Lad.-fl. — Ladoga-Ilmen area Up.Dn. — upper Dniester area Caucasus N.Cau. — Northern Caucasus Western Siberia (W. Sib.) E. Ural — eastern slope of the Urals Far East (F. E.) Kam. — Kamchatka Sakh. — Sakhalin N. Sakh. — northern Sakhalin S.Sakh. — southern Sakhalin Central Asia (C. Asia) Aral-Casp. — Aral-Caspian area N. Aral — northern Aral area TRANSLATION EDITOR'S NOTE Stratigraphic terminology in the Soviet Union differs somewhat from the accepted international terminology. In order to avoid any possible confusion the original Russian strati- graphic terminology has been retained in this translation. Thus, "tsvita" is rendered suite (and not formation), 'formatsiya' is given as formation, etc. For a discussion of the significance of these terms and the generally accepted equivalents the reader is referred to ''Report of the Twenty-First Session of the International Geological Congress. Part XXV: Stratigraphic Classification and Terminology," Det Berlingske Bogtrykheri, Copenhagen. 1961. 9 10 I. GENERAL PART 1, HISTORY OF STUDIES OF SILICOFLAGELLATES The term Silicoflagellatae was introduced by Borgert in 1891, although these organisms were known much earlier. The first report concerning the group was made by Ehrenberg to the Berlin Academy of Sciences in 1838. In a study of the microscopic structure of ''cretaceous rocks" in Sicily Ehrenberg found numerous skeletons of a peculiar nature, which he named as anew genus Dictyocha inthe class Polygastrica (Ehrenberg, 1839). Ehrenberg also found the first living forms of the group in the plankton of Kiel Bay. He described tens of species of silicoflagellates after examining numerous specimens of rocks from Africa, Italy, Greece, India, North America, as well as plankton and bottom samples from the North Sea, the Baltic, the Mediterranean, Black Sea, Caspian Sea, Sea of Japan, China Sea, the Sea of Okhotsk, and the Atlantic Ocean (Ehrenberg, 1839, 1841, 1844b, 1854, 1873). Most of these species have no more than historical significance today. During the first half of the 20th century, research on silicoflagellates was mainly taxonomical. Because of the rather limited distribution of these organisms in present-day seas, attention was focused on fossil materials which provide an abundant variety of forms. Thus, Lemmermann (1901b) based his classification on a study of a large amount of living and fossil silicoflagellates. The review by Schulz (1928) and the monograph by Gemeinhardt (1930) contain descriptions of many silicoflagellate forms together with data on their distribution in present-day seas and in Cretaceous to Quaternary deposits in Europe, Asia, Africa, North America and New Zealand. The new classification of silicoflagellates by Frenguelli (1940) is based entirely on fossil material. In addition to taxonomical works, a number of morphological and biological studies of the group have appeared (Gemeinhardt, 1930, 193la,b, 1934; Hovasse, 1932; Marshall, 1934; Frenguelli, 1935, 1938a,b; etc.). Research on morphology and biology of some silicoflagellates led to changes in the classification of these organisms. Ina study of the morpho- logy and nutrition of a living species of the genus Hermesinum of the order Stereotestales established by Lemmermann (1901a,b), Hovasse (1932) demonstrated the absence of chromatophores and the presence of two flagella. On these grounds, Deflandre (1951) placed the order Stereotestales in a separate group Ebriideae. According to Deflandre, these primitive heterotrophic flagellates are much closer to radiolarians than to siliceous flagellate algae for which he reserved the name silicoflagellates. 11 Deflandre made major contributions to our knowledge on silicoflagellates. His works (see bibliographical list) deal with various aspects of the morphology, taxonomy, geography, ecology, evolution and phylogeny of the group. With the development of micropaleontology research on silicoflagellates received a new impetus. The well-known micropaleontologist Hanna (1928a) wrote that silico- flagellates are excellent indicators of the age of marine sedimentary rocks, since most species of the group occupy a brief span of geological time and possess a wide geographical distribution. However, the use of silico- flagellates as a stratigraphic tool is only a recent development. The article by Colom (1952) contains a list of the silicoflagellates found in the Aquitanian- Burdigalian deposits of Spain and represents an attempt ata reconstitution of the paleogeographic conditions of that time on the basis of the ecology of the group. Desikachary and Maheshwari (1956) studied the fossil silicoflagellates of India. Ichikawa (1950, 1956) described silicoflagellates from various strata of the Neogene of Japan. Tynan (1957) published a detailed analysis of the remains of the silicoflagellate flora of the Calvert formation (Middle Miocene) in the state of Maryland. Mandra is working on the silicoflagellates of the Cretaceous, Paleogene and Neogene of California. In a number of brief communications, Mandra (1951, 1954) confirmed Hanna's view of the great value of silicoflagellates to strati- graphy. Ina report of his research in fossil silicoflagellates, Mandra (1960) established the silicoflagellate complexes characteristic to the Maestrichtian stage, the Late Eocene, Miocene, and Miocene- Pliocene using statistical analysis. He also determined the similarities and differences between these complexes, indicating that silicoflagellates can be used for stratigraphic differentiation and correlation of deposits. In his handbook of stratigraphy, Papp (1959) noted that silicoflagellates can be used quite reliably for distinction between Paleogene and Neogene deposits. Stradner (1961) reported on the Oligocene silicoflagellates of Austria. Other publications deal with the Tertiary silicoflagellates of the Vienna basin (Bachmann, Papp and Stradner, 1963). Bachmann and Ichikawa (1962) described the silicoflagellates of the Neogene of Japan. Tsumura (1963) studied the classification of the group, but made no mention of the geological distribution and evolution of the forms described. Only a few special works on silicoflagellates have been published in the USSR. Zhuze (1949a, 1951, 1955) has described several silicoflagellate species from the Upper Cretaceous and the Paleogene of the eastern slope of the Urals, and the West Siberian plain. Ina rather long article, Proshkina- Lavrenko (1959) dealt with the morphology, geography and ecology of silicoflagellates and made an interesting comparative charac- terization of the Recent and Neogene silicoflagellate floras of the Black Sea basin. In a number of articles, Glezer (1959, 1960, 1962) reported on the study of fossil silicoflagellates in the Paleobotanical Laboratory of VSEGEI. The first of these articles contains a detailed description of the family Vallacertaceae Defl., characteristic of the Cretaceous, from materials from the eastern slope of the Urals. The second article deals with the evolution of silicoflagellates in the Paleogene of the eastern slope of the Urals and the West Siberian plain, while the third article discusses the evolution and phylogeny of the group. 12 Information on silicoflagellates can be found in many publications on the phytoplankton of present-day seas (Palibin, 1903—1906; Usachev, 1927, 1935, 1946, 194 7ayb, 1949; 196 1>. Kigeley,.1925, 1928, 4031.) 1935a: 1937, 1939, 1953, 1957, 1959a,b; Morozova-Vodyanitskaya, 1940, 1948, 1954; Gail, 1950; Kuz'mina, 1959, 1962a,b; Semina, 1959, 1960; Korotkevich, 1960), as well as in articles dealing with fossil diatoms (Gaponov, 1914, 1915; Sheshukova-Poretskaya, 1955, 1959, 1961; Cheremisinova, 1957, 1959; Galerkina, 1959; Strel'nikova, 1960; Krotov, Shibkova, 1961; etc.). Bibliographies on silicoflagellates can be found in the works of Schulz (1928), Gemeinhardt (1930), Deflandre (1950), Hanna (1957), and Proshkina- Lavrenko (1959). 2. GENERAL CHARACTERISTICS OF SILICOFLAGELLATES MORPHOLOGY Although the cytoplasmic structure of silicoflagellates has hardly been studied, the morphology of the skeleton is known in detail. As a rule, the silicoflagellate skeleton consists of hollow, tubular siliceous rods. Some authors (Deflandre, 1950) assume that the skeleton is filled with seawater, while others (Lemmermann, 1901b) believe it contains air which reduces the specific weight of the cell and represents a major adaptation for rising in the water column. The outer surface of the skeleton is marked with fine spines, tubercles and ribs. Their arrangement and size vary according to species and also according to the age of the cell; in young cells these elements are much less developed than in older ones (Figure 1, 1) (Deflandre, 1940c). The ornamentation of the skeleton surface has been studied very little. In most species the skeleton appears as a subpyramid (Figure 1, 2), the base of which consists of a basal ring composed of basal rods. The basal ring varies with the species; it may be rounded, oval or polygonal. From the poles or corners of the basal ring arise outgrowths — radial horns (or spines) (Figure 1, 2—9, rh), which may be inconspicuous or very coarse and long. According to Lemmermann (1901b), the length of the radial horns depends on the temperature conditions: organisms living in cold waters develop much longer radial horns than those found in warm waters. Schulz (1928) associates the length of the radial horns with the salinity of the water: the lower the salinity, the longer the horns. Hovasse (1932) believes that the development of the radial horns depends somehow on the physicochemical conditions of the fixation of silicon. Gemeinhardt (1934) has found a close relationship between the length of the radial horns and the density and illumination of the water. In high latitudes, long radial horns are developed in spite of the high density of the water since normal photosynthesis requires that the cells rise up to the upper, better illuminated layer of water. 13 FIGURE 1. Nomenclature of the silicoflagellate skeleton: 1 —reticulate surface of silicoflagellate skeleton (detail) (Deflandre, 1950); 2 — Dictyocha fibula Ehr. var. fibula f. fibula (lateral view); 3 — D.tria- cantha var. apiculata Lemm. f. apiculata (apical view); 4—D. fibula var. aculeata Lemm. (apical view); 5—D.deflandrei var. bicornuta Gleser (ventral view); 6—Naviculopsis biapiculata var. constricta (Schulz) Gleser (apical view); 7—Distephanus speculum (Ehr.) Hack. var. speculum (apical view); 8 —D. s. var. cannopiloides (Pr.-Lavr.) Gleser(apical view); 9—Cannopilus hemisphaericus (Ehr.) Hack. (apical view); 10— Dictyocha fibula Ehr. (Marshall, 1934) (cell). br —basal rod; bw —basal window; rh —radial horn; lr — lateral rod; ar — apical rod; ap — apical plate; ak — apical ring; aw — apical window; ss — supporting spine; as — accessory spine; ec —extraskeletal cytoplasm; c —chromatophores; p — pseudopods; f — flagellum. The top of the pyramid is referred to as the apical apparatus. In the simplest case, this consists of a tubular apical rod (or trabecula) (Figure 1, 4 ar) or a markedly flattened apical plate (Figure 1, 5,6, ap). A more complex apical apparatus is composed of several apical rods which form an apical ring (Figure 1, 7, ak) with a single apical window 14 (Figure 1, 7, aw). A more complicated structure of the apical apparatus involves the development of numerous apical rods enclosing many apical windows (Figure 1, 8,9). The apical apparatus is linked with the basal ring by means of lateral rods (Figure 1, 2—5,7, 8,1r) which divide the basal ring into several basal windows (Figure 1, 2—8,bw). The basal rods bear supporting spines (Figure 1, 2—5,8,ss), directed obliquely downward. The position and size of these spines differ among species. The supporting spines are usually attached directly below the lateral rods in ancient forms and reach a relatively larger size than in the more recent species. These spines support the cytoplasm from below. The apical apparatus is often equipped with accessory spines (Figure 1, 4,7, as). The silicoflagellate skeleton shows a remarkable degree of variation. Deflandre (1950) tried to classify the different types of skeletal variation. He distinguishes among 3 groups: 1) mutants — symmetrical forms which differ considerably from the original type (Deflandre,l.c., Figure 197); 2) premutants — assymetrical forms intermediate between the respective type species and the mutant (Deflandre, l.c., Figure 196); 3) anomalies — clearly teratological forms (Deflandre, l.c., Figure 216). Different skeletal elements, such as radial horns, supporting and accessory spines, apical apparatus and even the basal rods, may be completely absent. The basal ring and apical apparatus vary in structure independently. Among the most stable signs are the form and size of the basal ring. The number of basal rods varies widely due to splitting of the basal ring at the corners where new rods are formed (Deflandre, 1950, Figures 98—106). Various forms of apical apparatus in silicoflagellates have been described in detail by Hovasse (1932) and Frenguelli (1935). Often these authors give clearly teratological signs as evidence for far-reaching conclusions about the classification of silicoflagellates, especially in relating some species of Distephanus Stohr to the genus Dictyocha Ehr. An essential short- coming of studies of variation of living silicoflagellates is the lack of experimental evidence for the views expressed. The modern concepts of the structure of the cytoplasm of silicoflagellates are based on observations of Borgert (1891) and Gemeinhardt (1930) on Distephanus speculum (Ehr.) Hack., the work of Hovasse (1932) on Dictyocha fibula Ehr. and Distephanus octonarius (Ehr.) Defl., and Marshall (1934) on Dictyocha fibula Ehr. and Diste- phanus speculum (Ehr.) Hack. The cytoplasm occupies the space enclosed by the basal ring, the apical apparatus and the supporting spines. Externally the skeleton is lined with a layer of cytoplasm (Figure 1, 10,ec). The extraskeletal cytoplasm of Dictyocha fibula Ehr. is more developed than that of Distephanus speculum (Ehr.) Hack. (Marshall, 1934). Hovasse (1932) was unable to detect any such cytoplasm in Distephanus octonarius (Ehr.) Defl.; Deflandre (1950) states that this species has an extremely thin layer of extraskeletal cytoplasm. There is no differentiation of the cellular membrane. The form of the cell depends entirely on the skeleton. The nucleus is situated in the center of the cell; by suitable staining, a central caryosome, peripheral chromatin and a nuclear membrane can be detected. Small, yellowish brown or greenish brown chromatophores are scattered in the cytoplasm (Figure 1, 10,c). The chromatophores of Distephanus speculum (Ehr.) Hack. sometimes merge into a rosette 10 15 at the base of the radial horns (Marshall, 1934). The cytoplasm contains numerous inclusions in the form of small, highly refractile droplets, 1—3y in diameter, which do not stain with iodine or osmic acid and may be assumed to contain the storage substance leucosin. The flagellum, located near one of the radial horns (Figure 1, 10, f), propels the cell by a rotatory movement. At the ends of all or 1—2 of the radial horns, the cytoplasm sometimes forms thin, filiform motile pseudo- pods (Figure 1, 10,p) reaching a length of 50yu. Hovasse (1932), who has observed the pseudopods of cells during reproduction, assumes that these structures participate in secretion of the skeleton. Deflandre (1950) re- gards the pseudopods as an adaptation for vertical movement in the water. REPRODUCTION Silicoflagellates reproduce by simple division. Prior to division, a daughter skeleton develops close to the maternal one. After a study of cell division in Distephanus speculum (Ehr.) Hack., Gemeinhardt (1930) concluded that the formation of the daughter skeleton is initiated at the apical ring and ends at the basal ring. Hovasse (1932) maintains that all the elements of the daughter skeleton of Distephanus speculum (Ehr.) Hack. and Dictyocha fibula Ehr. develop simultaneously. The formation of the daughter skeleton of Distephanus octonarius (Ehr.) Defl. proceeds in 2 phases. First formed is the basal ring, which is a mirror image of the basal ring of the maternal cell; at the ends of the ring the radial horns appear and reach the length of the maternal counterparts before thickening. The formation of the daughter skeleton often ends ai this stage, with the formation of a Mesocena-like skeleton. Normally, however, the apical apparatus appears after formation of the basal ring and radial horns. The lateral rods appear first, and then the apical rods and sometimes the accessory spines. The development of the daughter skeleton is concluded with the formation of the supporting spines, after which the developed daughter cell separates from the maternal cell, although the two skeletons sometimes remain firmly bound. Such double skeletons have been described in many species, such as Distephanus speculum (Ehr.) Hack. (Gemeinhardt, 1930); Dictyocha navicula var. biapiculata Lemm. (= Naviculopsis biapiculata (Lemm.) Freng.), D. triacantha var..inermis Lemm. and some other species (Schulz, 1928) and D.fibula Ehr. Hovasse (1932). Borgert (1891) and Schulz (1928) regard this phenomenon as copulation, while Gemeinhardt (1930) considers it support for the view that the silicoflagellate skeleton consists of two halves. Hovasse (1937) obtained several triple skeletons in the Bosphorus, one of which was not developed and consisted of the basal ring only. ECOLOGY Very little is known on the ecology of silicoflagellates. This lack of knowledge may be due to the negligible role of silicoflagellates in the 16 present-day seas. Indeed, only two silicoflagellate genera — Dictyocha Ehr. and Distephanus Stohr — have been obtained with certainty from these seas. Even under the most favorable conditions, silico- flagellates account for no more than 0.155% of the number of planktonic organisms in Kiel Bay (Brandt, 1898). In Oslo Fjord, Gran (1915) obtained up to 50,400 organisms of Distephanus speculum (Ehr.) Hack. per liter water. The density of the same species in the Black Sea was found to vary from 176 to 2,888 cells per liter (Morozova- Vodyanitskaya, 1954). Silicoflagellates are typical inhabitants of the marine and oceanic plankton, and are encountered in all the oceans and seas of the globe, but are not known from inland salt waters; in the Caspian Sea, they probably represent Tertiary relicts. Thus, the adaptability of silicoflagellates to such factors as temperature and salinity of seawater is relatively great. The quantitative development of silicoflagellates depends primarily on temperature and salinity conditions. Thus, Distephanus speculum (Ehr.) Hack. is rare in the eastern part of the Baltic Sea where salinity is lower than 10% (Schulz, 1928), whereas considerable numbers of this silicoflagellate are found at salinities over 20% (Gemeinhardt, 1934). The optical salinity for these organisms is 30—40% (Gemeinhardt, 1930). Hovasse (1932) found that silicoflagellates can withstand a lowering of salinity to 18%. Distephanus speculum (Ehr.) Hack. lives in the open waters of the Black Sea at a salinity of about 18%, while Dictyocha fibula Ehr. occurs in the strongly freshened northwestern part of the same basin (Proshkina-Lavrenko, 1959). The optimal temperature for Distephanus speculum (Ehr.) Hack. is close to 0°C (Gemeinhardt, 1931la), while that of Dictyocha fibula Ehr. ranges from 18 to 20°C (Gemeinhardt, 1934). Mass development of Dictyocha fibula Ehr. has been found in equatorial waters (Stiiwe, 1909), but smaller amounts of this species are encountered at lower temperatures. Thus, Vanhdffen (1897) obtained isolated specimens of D.fibula Ehr. from the coastal waters of Greenland, while Gemeinhardt (1934) encountered the same species in fjords along the west coast of Norway at temperatures lower than 10°C and in the southern Atlantic at temperatures below 4°C. In collections by Loman in Weddell Sea at 70— 72° S at a temperature of 1—1.87°C, 98% of the silicoflagellates were Distephanus speculum (Ehr.) Hack., whereas Dictyocha fibula Ehr. accounted for only 2% and was absent from some samples. The South Polar Expedition did not encounter D.fibula Ehr. at temperatures lower than 16.5°C (Gemeinhardt, 1931la). Hovasse (1932) states that the lowest temperature at which D.fibula Ehr. can be found in the Bosphorus is 14°C. Semina (1960) is inclined to regard D.fibula Ehr. as a boreal species. Another warmwater species is Distephanus octonarius (Ehr.) Defl., whose thermal optimum does not differ from that of Dictyo- cha fibula Ehr. (Hovasse, 1932; Deflandre, 1950). Gemeinhardt (1934) regards Distephanus crux (Ehr.) Hack. as intermediate between the warmwater species Dictyocha fibula Ehr. and the cold-water species Distephanus speculum (Ehr.) Hack. Like all phototrophic organisms, silicoflagellates require a certain level of illumination for normal development. In high latitudes where the light intensity is low, maximal numbers of these organisms are found near the surface. Gran (1927) found the main mass of the silicoflagellate population of the coastal waters of Norway in the water layer between the surface and 17 1-m depth, although an appreciable number of specimens were found to a depth of 50 m. In the equatorial zone of the southern Atlantic, Dictyocha fibula Ehr. (which forms nearly all of the silicoflagellate flora there) occurs mainly at a depth of 15—70 m (Stiiwe, 1909). In the Black Sea, the silicoflagellate population is twice as dense at a depth of 50 —100 m than at 0—50 m (Morozova-Vodyanitskaya, 1954). Little is known about the seasonal development of silicoflagellates. In the Baltic Sea,the Atlantic and the coastal waters of Norway the peak of Distephanus speculum (Ehr.) Hack. appears together with prolifera- tion of dinoflagellates in the fall; during the rest of the year the silico- flagellates are very rare (Gemeinhardt, 1930). In the Norwegian fjords, Dictyocha fibula Ehr. occurs during the summer (Jérgensen, 1905). 3. INTRODUCTION TO THE SYSTEMATICS OF SILICOFLAGELLATES POSITION OF SILICOFLAGELLATES AMONG THE ALGAE It is generally agreed today that silicoflagellates are algae. This was finally proven by Borgert in 1891, more than 50 years after the discovery of the group by Ehrenberg (1839). Ehrenberg described a vast number of species for which he established the genera Dictyocha Ehr. and Mesocena Ehr., which he placed together with diatoms ina class of infusorians — Polygastrica Ehr. Kiitzing (1849, 1865) considered the genera Mesocena Ehr. and Dictyocha Ehr. to be diatoms, but placed them in a separate family Actinisceae Ktz. (Order Appendiculatae Ktz., Tribe Diatomeae areolatae Ktz.) because of their peculiar morphology. While Ehrenberg and Kutzing considered the species Mesocena Ehr. and DictyochaEhr. independent organisms, such prominent German zoologists as Miller (1855), Hackel (1862, 1887) and Hertwig (1879) interpreted the silicoflagellate skeletons as parts of the skeletons of large radiolarians. This viewpoint is best reflected in Hackel's major monograph on radiolarians (Hackel, 1887). Hackel placed the 4 silico- flagellate genera known at the time (Dictyocha Ehr., Mesocena Ehr., Distephanus Stohr, Cannopilus Hack.) in the subfamily Dictyochida Hack. (family Cannorhaphida Hack., order Phaeocystina Hack., legion Phaeodaria Hack. or Cannopylea Hack., subclass Ocylosa Hack., class Radiolaria). Even after Borgert's publications appeared, some authors (Cocco, 1904— 1905; Martin, 1904) continued to agree with Hackel. After a thorough study of the morphology of living cells of Distephanus speculum (Ehr.) Hack., Borgert (1891) proved their affiliations to algae and placed them in a separate group which he named Silicoflagellatae. Although the classification and taxonomic ranks assigned to silico- flegellates differ among authors, it is widely held that these forms belong to the Chrysophyceae. Lemmermann (190la, b), Schulz (1928) and Gemeinhardt (1930) place silicoflagellates in the family Chrysomonadinen of the type Flagellatae; Fritsch (1948) in class Chrysophyceae of the type Algae; Kursanov (1953) in the class Chrysomonadinae of the type Flagellatae 18 under the name of the order Silicoflagellatae; Krishtofovich (1957) regards Silicoflagellatae as a subclass of the division Chrysophyta; Fott (1959) considers the suborder Silicoflagellineae of the order Chrysomonadales of the class Chrysophyceae of the type Chrysophyta; finally, Némec (1959) places the suborder Silicoflagellinae in the order Chrysomonadales of the division Monadophyta. Deflandre (1950) has a somewhat different view of the systematic position of silicoflagellates. He believes that the peculiar structure of the silico- flagellate cell warrants the establishment of a separate class belonging to the flagellates; at the same time, he relates the silicoflagellates to the chrysomonads and coccolithophorids. These concepts have been adopted in various books on zoology (Grassé, 1952), paleontology (Piveteau, 1952; Moret, 1958) and paleozoology (Muller, 1958). It is difficult to find any particular relationships between silicoflagellates and any other algal group. No other alga known to science has a siliceous endoskeleton such as the silicoflagellate. Indeed, silicoflagellates area unique taxonomic entity deserving the rank of class. The presence of a single flagellum, brownish yellow chromatophores and reserve food substances of the leucosin type all suggest a phylogenetic link with the Chrysophyta. PRINCIPLES OF CLASSIFICATION OF SILICOF LAGELLATES The classification of silicoflagellates is based entirely on the structure of the skeleton. The taxonomic value attached to various morphological signs has varied in the course of time, which has led to corresponding alterations in the volume of the species and genera. Ehrenberg placed all the forms with a simple, ring-shaped skeleton in the genus Mesocena Ehr., and reserved the genus Dictyocha Ehr. for those with a skeleton shaped like a reticulate star. The smallest deviations in skeletal structure, even in an individual specimen, prompted Ehrenberg to establish new species. Hackel (1887) divided the genus Dictyocha Ehr. on the basis of the structure of the apical apparatus into Dictyocha Ehr. proper, Distephanus Stohr and Cannopilus Hack. Hackel's definition of the silicoflagellate genera was fully accepted by Lemmermann (1901b, 1903, 1908), Schulz (1928), Gemeinhardt (1930) and others. Lemmermann (1901b) published a revision of all the silicoflagellate species described by Ehrenberg. This revision was based mainly on the number of sides of the basal ring (the genera Dictyocha Ehr. and Distephanus Stohr) and the number of apical windows (Cannopilus Hack.). The size of the basal ring, the presence or absence of radial horns, and sometimes the number of sides of the basal ring served as bases of differentiating yroups below species rank for Lemmermann. The same morphological features play a guiding role in monographs by Schulz (1928) and Gemeinhardt (1930). Quite different systematic principles serve as the bases for the classi- fications of Frenguelli (1940) and Deflandre (1950), who believe that the 19 structure of the apical apparatus is too variable and unstable to be used as a taxonomic guide, especially on the generic level. The genera established by these authors are based less on the general form of the skeleton than on the position of the supporting spines (the genera Dictyo- cha Ehr. and Corbisema Hanna), the direction of the radial horns (the genus Cannopilus Hack.), the trend to a reduction of the apical apparatus (the genus Paradictyocha Freng.), the flattening of the basal rods (the genus Naviculops Freng.), etc. In the description of the species, Frenguelli attributes considerable importance to the size of the skeleton. Thus, the only difference between Dictyocha fibula Ehr. (Frenguelli, 1940, Figure 1,f) and Distephanus speculum Enhr. (Figure 1, a—e) consists of the greater skeletal dimensions of the former, while morpho- logical differences between the two species are not considered at all. Stressing the great variation among silicoflagellates, Frenguelli and Deflandre point out that externally similar forms — Mesocena-like, Distephanus-like, Cannopilus-like, etc. — may occur in a large number of species, even of different genera. Such forms are merely an expression of the variation of the species and should not be treated as separate taxons. For this reason, Frenguelli and Deflandre attacha considerable importance to the locality and phylogenetic links of the described forms, and morphological differences are often relegated toa secondary place. Thus, Deflandre (1950, Figure 190) places in Dictyocha frenguelli Defl. the triangular forms with accessory spines found in the Eocene of the Volga area, while describing closely similar forms from the Oligocene — Miocene of Barbados Island (Deflandre, 1950, Figure 178) as a new species, Corbisema spinosa Defl. After the discovery of an intermediate form between Dictyocha navicula Ehr. and D. triacantha var. inermis Lemm., Deflandre united the two under the name of Corbisema apiculata var. inermis Lemm. (Deflandre, 1950, Figures 86—88). Deflandre (1950, Figures 241—243) classifies as Naviculopsis navicula (Ehr.) Defl. skeletons (analogousto Dictyocha navicula Ehr.) from the Miocene of Greece. Using the phylogenetical approach, Deflandre (1950, p. 67, Figures 194 —202) united a number of forms in Dictyocha ausonia Defl., which had earlier been placed in different species and even genera. Frenguelli and Deflandre can be credited with attempting to introduce the phylogenetical method in the classification of silicoflagellates, although the lack of clear-cut morpho- logical differences between the taxons and the frequent use of a single trait as a crucial sign detract from the practical value of their systems. My own classification of silicoflagellates is based essentially ona combination of morphological signs. Wherever possible, in addition to morphological aspects, phylogenetical and geochronological criteria are considered. Thus, in the discussion as to whether the genus Distephanus Stohr should be retained as a separate taxon or united with the genus . Dictyocha Ehr., as suggested by Frenguelli (1940) and Deflandre (1950), the following facts were taken into account: 1) the genus Distephanus Stohr appears in the Eocene, while species of the genus Dictyocha Ehr. are known since the Cretaceous; 2) the Eocene representatives of the two genera show marked morphological differences from one another and no transitional forms have been found; 3) the reduction of the apical ring in some species of Distephanus St6hr is confined to Neogene and Recent forms and is usually accompanied by a mass proliferation together with a considerable variation in the skeleton. 15 In other words, the similarity between the apical apparatus of some Distephanus Stohr skeletons and the simple apical rod characterizing the genus Dictyocha Enhr. is in my view a secondary phenomenon and does not justify a union of the two genera. In establishing the new species Dictyocha lamellifera Gleser, I took into account the general configuration of the skeleton, some details in the structure of the basal rods and the fact that these forms are associated mainly with Early Eocene deposits of the Volga area, the eastern slope of the Urals and Denmark. Schulz (1928) and Gemeinhardt (1930) placed this form in D. triacantha Ehr. because of the number of sides of the basal ring. Entirely on the basis of the details of the structure of the basal rods, Frenguelli (1940) regards the skeletons of this species as a triangular form of Naviculopsis biapiculata (Lemm.) Freng. I believe that only a comprehensive approach based on a number of morphological signs and geological data can prove the independence of Dictyocha lamellifera Gleser. Indeed, by considering a number of signs instead of any single feature one sees clearly that this species differs sharply from both D.triacantha Ehr. and Naviculopsis biapiculata (Lemm.) Freng., although it shows similarities to each of them. A study of the evaluation of Dictyocha lamellifera Gleser shows that this silicoflagellate occasionally occurred together with the above two forms, but flourished during a quite different time. The combined use of the morphological and evolutionary methods in the classification of silicoflagellates allows not only a comparison of forms from remote areas, but also an analysis of the evolution of the whole group. CLASSIFICATION OF SILICOFLAGELLATES The first classification of silicoflagellates was proposed by Lemmermann (190la, b). It consisted of two orders, Siphonotestales and Stereo- testales.* Siphonotestales included a single family Dictyochaceae with 4 genera — Mesocena Ehr., Dictyocha Ehr., Distephanus Stohr and Cannopilus Hack. Later Schulz (1928) placed in Dictyochaceae the genus Cornua Schulz, for which Gemeinhardt (1930) created the new family Cornuceae. The classification by Lemmermann, adopted and developed by Schulz and Gemeinhardt, reflects the progressive complication of the silico- flagellate skeleton from the simple basal ring of the genus Mesocena Ehr. to the intricate skeleton of the genus Cannopilus Hack. However, it does not take into account the actual evolution of the whole group, since it begins with the secondarily simplified genus Mesocena Ehr. The family Cornuceae, consisting of the genus Cornua Schulz, occupies an isolated position in this system. The classification by Frenguelli (1940) contains a single family Dictyochaceae with 7 genera — Mesocena Ehr. emend. Defl., Para- dictyocha Freng., Dictyocha Ehr., Cannopilus Hack., Corbisema Hanna emend. Freng., Naviculopsis Freng. and Clathrium Freng. The arrangement of the genera in this classification * The order Stereotestales, later separated into the simpler group Ebriidea, is not discussed here. 16 20 is formal, and as in the previous classification does not reflect the evolutionary process. By contrast, the classification proposed by Deflandre (1950, 1952a, b) reflects his views on the evolution of silicoflagellates. Deflandre published two classifications — one for living and another for fossil forms. The living group consists of only 3 species, all of the genus Dictyocha Ehr. The fossil system is more complex. Dictyochidae, the most primitive family according to this classification, consists of 8 genera: Corbisema Hannaemend. Freng., Dictyocha Ehr., Paradictyocha Freng., Mesocena Ehr. emend. Defl., Naviculopsis Freng., Cannopilus Hack., Phyllodictyocha Defl. and Nothyocha Defl. Deflandre established the more advanced family Vallacertidae with 3 genera Vallacerta Hanna, Cornua Schulz and Lyramula Hanna. In addition, Deflandre placed the genera Clathropyxidella Defl., Clathrium Freng. and Pseudorocella Defl. ina group of uncertain taxonomic position. In a totally new classification, Tsumura (1963) established the new orders Cladotestales and Eutestales. In the former order Tsumura placed two families: Cornuacea Gem. with the single genus Cornua Schulz, and Lyramulaceae Tsumura with the single genus Lyramula Hanna. The order Eutestales consists of a single family Dictyochaceae Lemm. with the following 4 genera: Mesocena Ehr., Dictyocha Ehr., Diste- phanus Stohr and Cannopilus Hack. Tsumura abolished the genera Vallacerta Hannaand Naviculopsis Freng. by placing their species in Dictyocha Ehr., as did the taxonomists at the beginning of the 20th century when there were no data on the evolution of silicoflagel- lates. The classification proposed here is based on the following principles. 1. Living and extinct forms are classified collectively, since the systematics should reflect as fully as possible the phylogenetic links between the living species and their fossil ancestors. 2. Not only morphological traits, but also evolutionary and phylogenetic links of the orders, families and genera have been considered in the arrangement of these categories. My classification is as follows: Type Chrysophyta Class Silicoflagellatophyceae Borgert Order Vallacertales Gleser Family Vallacertaceae Defl. Genus Vallacerta Hanna Order Siphonotestales Lemm. Family Cornuaceae Gem. Genus Lyramula Hanna Genus Cornua Schulz Family Dictyochaceae Lemm. Genus Dictyocha Ehr. Genus Corbisema Hanna Genus Naviculopsis Freng. Genus Distephanus Stohr Genus Paradictyocha Freng. Genus Cannopilus Hack. Genus Mesocena Ehr. 17 21 In my view, the family Cornuaceae Gem. shouldinclude not only Cornua Schulz, but also the related genus Lyramula Hanna. The genus Vallacerta Hanna is so different morphologically from the remaining members of Class Silicoflagellatophyceae that it should be placed separately in the family Vallacertaceae Defl., which is attributed to the separate order Vallacertales Gleser. The two other families — Cornuaceae Gem. and Dictyochaceae Defl. — are characterized by a tubular skeleton and belong to the order Siphono- testales Lemm. 4, DISTRIBUTION OF ANCIENT SILICOFLAGELLATES ON THE TERRITORY OF THE USSR Siliceous deposits of ancient seas are widespread on the territory of the USSR, and these contain numerous skeletons of silicoflagellates which lived in these seas. By examining materials from different parts of the USSR it was possible to determine the silicotlagellate flora of the marine plankton of the Quaternary (Mga) age in the northwestern part of the USSR, the marine Paleogene basin in the southwestern part of the European USSR, the Miocene sea of the Northern Caucasus, the eastern Ural Sea of the Upper Cretaceous, various parts of the Paleogene seas on the territory of the West Siberian plain and the Turgai Gates, and different localities in the Far Eastern Neogene Sea. To demonstrate the contemporaneity of the ancient floras, stratigraphic data and results of the diatom analysis of the corresponding deposits have been used. The material is arranged mainly according to geographical areas from north to south and west to east. EUROPEAN [WESTERN] PART OF THE USSR Northwestern sector of the European part of the USSR Leningrad Region A sample of Mga clays from a depth of 13.0 —13.5 m in well 700 near Otradnoe station (from the collection of N. A. Rzhonsnitskaya) was examined. The characteristic complex of diatoms as determined by I. A. Kuptsova (Hyalodiscus scoticus (Ktz.) Grun. —5, Thalassiosira gravida Cl. (spores) —6, Th. excentrica (Ehr.) cl. —4, Chaeto- ceros sp.sp. (spores) —4, Coscinodiscus perforatus Ehr. — 4, Actinoptychus undulatus (Bail.) Ralfs—4, Rhabdonema arcuatum (Lyngb.)—5, Grammatophora oceanica (Ehr.) Grun. —6, Thalassionema nitzschioides Grun. 6) corresponds to the second phase of the Mga interglacial sea, that is, at the peak of its transgression (Cheremisinova, 1959). The silicoflagellates encountered are Dictyocha fibula Ehr. var. fibula f. fibula and Distephanus speculum (Ehr.) Hack. var. speculum. Both forms are noted as abundant in occurrence. 18 22 Southwestern sector of the European part of the USSR The presence of silicoflagellates was tested in samples from the Kiev and Kharkov suites of some areas of the USSR. Calcareous facies predominate among the rocks of the Kiev suite, although in marginal parts of the Dnepropetrovsk-Donets depression the Kiev suite consists of sandy facies. In the upper part of the suite (Bug horizon) the clay is slightly carbonate or noncarbonate. The Kiev suite is now dated inthe Late Eocene according to molluskan fauna (Klyushnikov, 1960). Klyushnikov (1958) divides the deposits of the Kharkov suite in two horizons. In the lower, the Ingulets horizon, he places glauconitic and siliceous sands, glauconitic sandstones, greenish gray noncarbonate clays, gaizes, tripolis and diatomites; the upper horizon consists of glauconitic sands interstratified with sandstones and clays. Klyushnikov (1960) writes that the deposits of the Kharkov ''stage'' of the Ukraine are poorly defined from a paleontological viewpoint. All the organic remains are associated with the Ingulets horizon. Only the mollusks have been studied, while fossil groups such as radiolarians, bryozoans and sponges have not been described at all. The stratigraphic position of the layers containing fossil diatoms is obscure. Local and Early Oligocene species predominate in the molluskan complex, although there are many forms which also occur in the Late Eocene Kiev ''stage.'' Because of this, Klyushnikov places the Ingulets horizon rocks in the Early Oligocene. On the basis of new data, Klyushnikov recently concluded that the rocks containing remains of diatoms and other siliceous organisms overlie calcareous marls and clays of the Dnieper substage and are covered on the marginal parts of the Dnieper-Donets depression by eroded silty sands and siliceous concretionary sandstones of the Ingulets horizon. The latter is the lower component of the Kharkov stage, and its rocks contain remains of the fauna of the Early — Middle Oligocene. Therefore, the layers with remains of siliceous organisms must belong to the very upper part of the Kiev stage — the Bug substage, and therefore the Late Eocene. Zhuze (1949b) and Uspenskaya (1950) place the diatoms of the Kharkov stage in the Early Oligocene. Zhuze (1949b) holds this view because of the marked similarity between the diatom flora of the Kharkov stage and the Early Oligocene flora of Oamaru, New Zealand. Recently, however, some authors date the Oamaru diatoms in the Late Eocene (Kanaya, 1957) or Late Eocene — Early Oligocene (Fleming, 1959). Kaptarenko-Chernousova (1960) places the diatom flora, described by Zhuze (1949b) as part of the Kharkov stage, in the Middle— Late Oligocene. Analysis of species composition of the diatom complex of the Kharkov stage indicates that most of the species are also known from the marine clays of the upper part of the Tas- Aran suite in the Late Eocene of the basin of the Irgiz River. Owing to this, it is not possible now to speak of the undoubted Oligocene age of a number of diatoms. We examined several specimens from the Kiev and Kharkov suites of the Dnepropetrovsk and Sumy regions (from the collection of M. V. Yartseva), from the Kharkov suite of Krasnyi Oskol in the Oskol River basin (from the collection of E. A. Cheremisinova), and from the village of Boromlya of the Sumy Region (from the teaching collection of the Department of Lower Plants at LGU). 19 23 Silicoflagellate skeletons were found in the Kharkov suite on the left bank of the Dnieper near Dnepropetrovsk (north of Nizhne-Dneprovskii Uzel station), in the village of Krasnyi Oskol, in the Sumy Region (Boromlya village), and in the Kharkov and Kiev suites of the villages of Staroverovka and Melovoe. Dnepropetrovsk Region Numerous and varied silicoflagellate skeletons were found in the gray- green clays of the Kharkov (?) suite in a well drilled on the slope of a crystalline massif on the left bank of the Dnieper, 6 km north of Dnepro- petrovsk. Well 12, north of Nizhne-Dneprovskii Uzel station (from the collection of M. V. Yartseva) Quaternary eolian deposits To adepthof 18.25 m. Fine gray and yellowish gray, argillaceous sands. Kharkov suite (?) — Pg? (?) 18.25—32.0 m Greenish gray fine argillaceous sands with glauconite. 32.0 —39.60m Greenish gray sandy clay containing glauconite, diatom frustules, sponge spicules and radiolarians. Kiev suite (?) — Pgs! (?) 39.60—40.25m Argillaceous sand with glauconite and small foraminifers. 40.25—40.50m Limestone with nummulites. 40.50—49.60m Gravelly, carbonate sand with mollusk shells and small foraminifers. Buchak suite (?)—Pg?" (?) From49.60m _ Sandy clay overlying argillaceous and carbonaceous sands with interlayers of brown coal. Yartseva found frustules of the diatoms Aulacodiscus excavatus A.S. and Arachnodiscus ex gr.indicus Ehr. in rocks of the Kharkov (?) suite at a depth of 32.0—39.60 m (Nesterenko, 1960). According to V. S. Sheshukova-Poretskaya (Yartseva, 1960), these layers contain valves of marine, mostly planktonic Eocene and Early Oligocene species of the Kharkov "'stage.'' Yartseva assumes that the relatively 20 (24) _ N on uoll -en[eAo aATIvI -tluenb “JaSe[) 07DI17NUW DUaI0SaW “lasayy (z[Myas) sou -1ul "AWA DyD]NIIdD1q sisdoj)NI1avNV “lesa]Q (taupe.ays) vsonzra]{ “JeA DYyJUvIvIA, “GQ “Z[NYIS vYyUDIDTaY “Gq ‘wing *§ pynqif “ieA “Ay DvpNQi{ vYyI0/h}021q “1aSe[ v7IVIIINW DUa0sa py “1asa[t) (aaupeiys) vsonraj{ “1eA “7 “Gq “DYJUDIVDIA? “J DYJUDIVIAZ “IPA “ING VYJUDIVIGZ “G ‘Z[NYIS vYyUVIDLaYyY “Gq ‘yng °j pyngif “deA “AYA ByNQil vDYyI0A}20q “Z[NYIS SIsUaNnsDWVO DUIIOSA [WY “WOE sna1iapydsiway snzidouun) (14g) “ZnNAI “IVA “MOVE (AYA) TNs9 snuvydajsiq *pyvynzidviq ‘ieA ‘Sudly ((wWway) vnjn21dn1q sisdojnjianyy “‘DYyjUuvIvI47 *{ DYJUDIDIAZ “IVA “IY VYJUDIVIA *“G “Lasay (‘[Ja({) Bsouids -q ‘ZINYOS vYJUDIDTaY “GQ “pyngyf ‘J Dpngyf “AeA “AY VINGIL DYyI0hj21q satoads S21P[[ABeY OTIS (eAasueX “A ‘W JO UONDaTTOO aYy1 WOI) UOTZOy yYsAoNadoidouq ‘TpLP pur ZI ST[aM Woy seydues Jo uoNeUTUIeXa DIdoosoIOTWI Jo sifNsay (2) auao - 08110 Ajieq RIOT] wo1eIp jo a8y SINS oD OD “4 9 OD NS SIN St TLIO N © oO uot] -en[PAa aAT1e1 -Tluenb “Bain) suaosayu sjauojdiq ‘unIg sunj1q7N4 10)50)8D Jy "uNIg, 0919]2q v4iIsojDWAD “BAOY —nysoayS avaauv{ piuosounydajg ‘9snOf Dipaw VIMIDUIAT ‘unIN Dpisif ‘eA snydsowfjod * 7 ‘unIg, wnsourjshoijod snjynviwapyy “AIO, WnjDdvIQns WN14D18924 J, 19S] }9 BAONNYSIYS siasaurjas vuo10D ‘1ase[ 4@ BAOYNYSVYS s7n7 -ppnaiaspf “| 14a77ay snyohjdourjoP “dog = vydojos9v sixfidoryjuvy “I4YQ sndup snosipour9s09 ‘asnOf avuIjaqvz “je D41ISOISSD]DY J “BAONNYSAUS VVUILI “CG ‘asnof snuviaoyanys sixfidounydaig ‘asnor s2wuofiajid vuisopodopnas gq ‘asnof Dysapow “q ‘asnoy vuiviy vaisopog “10SaTD }9 BAOUSSO, 07/29 DsISsopodopnasg *"SOTIOTIVA pue ‘zyy (ayy) D2VIINS “pW "1S 10 ‘AD sisuanupwvo + py "Sy Disnof “pW (é) §84 “‘alins ‘uNnIG sIjv4injIaqYyILD «v4Isoja py \(é)aoyieYy satoads saxaTdWiod WOIPIp ITIsTIAIOeIeEYD ase pue aims 2u0si] Ts SNODORI[ISIV O'8ss VWLy a1tuooneys yam Aejqo uael8 ystkein Izge—L'ce | ZEST aituooney{s yim Aejpo useB ystkeip |y'ce—-O'%E| ZI kB opoutry Keine ‘T ATSVL 21 25 small amount of Early Oligocene species indicates that the respective layers belong to the very lowest horizons of the Early Oligocene. In underlying deposits at a depth of 39.60—49.60 m, Yartseva defined a variety of foraminifers, most of them characteristic of the Late Eocene (Nesterenko, 1960). Yartseva (1960) places the fine-sand carbonate clays of Nizhne-Dneprovskii Uzel station in the upper half of the Late Eocene because forms found there (Nummulites orbignyi (Galeotti), N. prestwichianus R. Jones, N. prestwichianus var. granulata (de la Harpe)) are known only from such layers (Wemmel sands) of the Belgian basin. V.S. Sheshukova-Poretskaya and I examined two samples from the sandy clays of the Kharkov (?) suite from depths of 32.0 —35.7 and 35.7—39.2 m (sample 12). This material was prepared only from the coarse fraction washed for examination of the microfauna, since no rock was at our disposal. The results will therefore be examined for both samples together, especially since they also contain very similar algae. We found that the diatom flora of the Kharkov (?) suite of the Dnepro- petrovsk area is very similar systematically to the complex encountered in the same suite in the Ukraine, Voronezh and Kursk regions. A charac- teristic feature of the Dnepropetrovsk flora is its greater variety of species, among which are several forms of the order Pennales and a number of other species apparently not occurring in other areas. The age of the flora is difficult to determine. It differs considerably from the well-known Late Eocene floras of Western Siberia and California, but a more or less undisputed Early Oligocene diatom flora is not known at present. Some authors stress the close similarity between the flora they studied and the marine Paleocene clay complex of the Tas- Aran series of the Middle — Late Eocene of the right bank of the Uzen-Kairakty (a right tributary of the Irgiz) as well as with the flora of Oamaru, New Zealand. The Oamaru flora has recently been placed in the Late Eocene (Kanaya, 1957) or Late Eocene — Early Oligocene (Fleming, 1959). There are altogether 10 species, varieties and forms of silicoflagellates. As can be seen in Table 1, only Dictyocha hexacantha Schulz and D. fibula Ehr. var. fibula f. fibula show frequent (3) and rare (2) occurrence; the remaining forms are very rare. Among the latter we found a new species — Mesocena muticata Gleser. An analogous but poorer complex of algae was encountered in well 4741, 58.0 m deep, situated 30 km northeast of well 12 (Table 1). The five species, varieties and forms of silicoflagellates were very rare; among them was Mesocena muticata Gleser. Oskol River basin From this basin one preparation, no. 903 from the village of Krasnyi Oskol southeast of Izyum (from the collection of E. A. Cheremisinova), was examined. E. A. Cheremisinova (1956) encountered in the Oskol basin a number of species which characterize the upper (third) horizon of the Kharkov stage: Coscinodiscus obscurus auterop ice (from the collection of N.N. Milyukova) The outcrop lies on the right bank of the Malaya Sosva, 1 km above the bend around Cape Svyatoi, at a height of 8 m above the river level. Bluish gray clays of the Chegan suite emerge at the waterline. One sample of these clays, no. 84, was examined. The sample contained remains of a fairly uniform diatom flora and a comparatively varied silicoflagellate flora (Table 7). Among the diatoms were very abundant valves of Melosira sulcata (Ehr.) Ktz. (group of forms) and abundant Pyxilla gracilis Temp. and Forti. The remaining species were much less numerous. This complex can be placed with reservation in the Late Eocene — Early Oligocene. The silicoflagellate flora consists of 15 species, varieties and forms, most of them in considerable amounts. Dictyocha rotundara Jousé var. rotundata is very abundant, while var. secta Gleser of the same species is frequent. Naviculopsis biapiculata var. minor (Schulz) Gleser is abundant, var. biapiculata frequent. Considerable amounts of skeletons of some forms of Dictyocha frenguelli Defl. and D. deflandrei Freng. were found. D. transitoria Defl. is frequent. 47 ise) FIN OO 1D OD un N © Std on uoTl -Pnyead aaTIe} -Tauenb (eaoyndAT IW “IG «§n7NI439 DuUar0sa py ‘Jaso] (Z[NYIS) souzw “sea “Gq “NV ‘pyyjnaidyig “1eA *SUady (wwe) 27D)nI1d01q sisdojzna21avVy “‘TJ9d M24071suDs1 “Gq *1eseTH “([Joq) vsourds -q *1OSO[X) DJIaS “IBA “4 “GQ “DIDPUNJOL “IBA QSNOL DJDpUNjOL “Gq *1e098[5 vnbi]qo “Gq “1OSO[ 4) DJ4IIU] “J S17UaIDI “IBA “f{ 'G "squad -p2 "J JOS8[ sizuaivo “eA “f “Gg 117 -Janduat{ “IBA "[Joq iJjansuas{ ‘Gq ‘pngif *y vjngif ‘iva “IYA vINGQI{ “GC “10899 (IN acl eg D]Ja1mouniyH vjonposd *} vjajdwoo “1eA ‘p “Gq ‘1q10q go ‘dwley, 87719049 v771zAg "23] ‘unin snuod =| £3 4_ 234 -dwoa *} Jaso[s v7a]dwo2 “eA “p *q -019DUW “IBA 19]]20W snasipourssoj|' , & i “10Se[) “(SuIO} Jo anys ELS DjNUL0I1Q “BA 1a4puDj{ap vYI0AI21q dnoiz)*zyy (ay) v709Ns Dursopayy| ueBeyD]| Avss ystntE uon -eny[eaad satoads P1OTJ satoads ; aaTle1 ase wi uw101eIp : ASojounty ; -tuenb pure aims uyidoq jo o8y S$OILT[IBeTJOOTIS soxa]d Wood WOIPIp OTIstTIAIOeIeYD "N‘N Jo UoTIOSTIOO ayI WoIy) IDATY eASOS [sassoT] eAeTEW ‘pg dosr9Ino Woy o[dues v Jo stskteue IIdoososIOTW Jo sitMsaYy *L AIGVL 48 ‘pypjnjidpig “IRA “SUdLy I (‘wuley) 70j)NI1d02q ale ea *p4iafi] ‘asnof szsuappun “9 Zz -]auD] “ABA JaSo[y VAaf7jJawy? “Gq ‘unin snuod | “JOST VJ1GIUI “| SI7UALVI “TRA *{ “G -OLIDU “IRA 249]]90W SnIsipoU1Ise) *s1quauva “| JASaT 29004 ‘(SuLI0J Jo ¢ $1]UILDI “IRA 1297ANSUaL{ DYI0A}2q ()e1ppIW dnois) ‘zy (IY) v7VI7INS viIS0]a J “IOS9TH (Z[MYOS) LouW2wW "IBA “Q “A ‘pyvjnjidvig “leA “Buddy J (‘wueTyT) v70jnI21d02q sisdoj)naI1avN | ‘TJod visojsuvs, “GQ J ‘DIDPUN}OL “IBA BSHOL VIVPUNIOL ‘CG ‘Dial ‘unig snsod ] -1]]9WD] “IBA JASA[D VAaf17]aWID] *q -O1IDU “IBA 140]]20Ul SnasipoUrIs0) if “LOSI VJ19IUI *} S2ZUALDI a ata Pee ‘unding) 22Y9801g sixfhdounydaig ‘naqjansuas{ *(SuIOJ Jo J “RA [JOC MpJansuesf vys0hj21q a1e7] dnoi8)*zyy (ay) Y7VI7NS vI1S0]a uoll uoTi coe sotoads Ploy egies satoads A181 Ate wo1eIp - b nuen esky -tquenb SOV [ABeEYOOTTIS SOXo[duIOd WOIkIp ITISTIBIOvIeYO (1] “d*d JO uoTIOaTTOO ay’ Woy) eae ATeyYIOYS ‘Y-LT pue 4-8 s{T[aM Woy satdues jo (50) 2 Ae 8d “altns JoAwT[NAT a11WI01PIq ert eared ‘o1Ins iz joawtpnky aiwoierq | 0'9ET ‘W-TI ase isa ASoyoyary oiduies pue a1mns pue [[9M uoTeUTWIeXS DIdoOosoOIOIW Jo si[Nsey *g ATAV.L 49 51 Area of the Sherkaly settlement From this area material of 4 wells (3-k, 5-k, 8-k and 11-k of the collection of P. F. Li) was examined. No algae were found in the first two wells. In wells 8-k and 11-k, diatoms and silicoflagellates were encountered in the layer of Eocene diatomites. As can be seen in Table 8, the diatom complex of well 8-k (depth 142.0 m, sample 1) is characterized by the presence of only 2 Coscino- diseus species — C. moelleri-var..maecroporus Grun. and C.uralensis Jousé. Both forms are abundant. This feature is reminiscent of Middle (?) Eocene flora known from the Lower Ob area. There are only 4 silicoflagellate forms. Only Dictyocha frenguelli var. carentis Gleserf. carentis is frequent; the remaining forms are very rare or rare. In well 11-k, remains of a very poor algal flora were found at a depth of 136.0 m (sample 2). Only frustules of Melosira sulcata (Ehr.) Ktz. (group of forms) are very abundant (Table 8). In its species composition, the diatom complex resembles the Late Eocene complex of the Malyi Atlym settlement (well 6-k, depth 320 m, sample 7, see below). The 7 species, varieties and forms of silicoflagellates determined are represented by very rare numbers (Table 8). Malyi Atlym settlement From the Malyi Atlym area materials from 2 wells — l-r and 6-k (from the collection of P. F. Li) were examined. Remains of algae were found only in samples from well 6-k. Well 6-k Chegan suite — Pg}— Pgi 39.3—220.1m Greenish gray clay, breaking down into irregular, thin- leaved pieces. 235.3—246.6 m_ Light greenish gray argillite, somewhat gaizelike, vaguely stratified, splitting into thin irregular plates. Lyulimvor suite — Pg}3 246.6 —264.1m_ Light gray, gaizelike argillite, in some places reminis- cent of diatomites. 283.0—333.5 m Light gray, loose, nonstratified diatomite. 341.5—347.8 m Gray, dense, monolithic gaize, breaking into large pieces. Five samples from the core were examined microscopically: no. 2 — greenish gray clays, depth 163.0 m; no. 3 — greenish gray argillite, 50 depth 240.0 m; no. 5 — diatomites, depth 287.0 m; no. 7 — diatomites, depth 320.0 m; no. 15 — gaize, depth 345.0 m. Remains of algae were found in samples 2, 3 and 7 (Table 9). Sample 7 contained remains of a well preserved diatom flora. The abundance of valves of species of Coscinodiscus suchas C. moelleri var. macroporus Grun. andC. payeri Grun., together with masses of Melosira sulcata (Ehr.) Ktz. (group of forms) and Grunowiella gemmata (Grun.) V.H., indicates that this complex belongs to the Late Eocene. Eight silicoflagellate taxons were encountered together with the Late Eocene (diatom complex). Three of these taxons — Dictyocha trenswellicvar/earentis Gleser igen retiis eta incerta Gleser and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata — were found in large numbers; the rest were very rare or rare. Samples 2 and 3 had a scarce and poorly preserved fossil diatom flora (Table 9) with Pyxilla gracilis Temp. et Forti as the dominant form; Melosira sulcata var. siberica Grun. is common and Stephano- PpYX1S _Marginata,Grun. very rare. This diatom complex is characteristic of the Late Eocene — Early Oligocene (?) deposits of the uppermost part of the Lyulimvor (Irbit) suite or the lower part of the Chegan suite. Both samples possess closely similar complexes of silicoflagellates in which Dictyocha rotundata Jousé var. rotundata dominates, and smaller amounts appear of Naviculopsis biapiculata var. minor (Schulz) Gleser. The samples differ in having Dictyocha transitoria Defl. anda greater amount of skeletons of D. rotundata var. secta Gleser in sample 3. In addition, the clays of sample 2 contain frequent skeletons of D. fibula Ehr. var. fibula, which is encountered in underlying argillites. Other differences involve individual forms. Basin of Pelym River near Burmantovo village Samples from wells 1, 5 and 15 were examined. The material from wells 1 and 15 contained only very rare, unidentifiable fragments of diatom frustules. Thesample from well 5, drilled inthe basin of the Pelym River, revealed remains of silicoflagellate and diatom floras. Well 5 Quaternary deposits 0.0—1.5 m Poorly graded, coarse, micaceous, gray sandstone and sand, with ferruginous spots, plant remains, gravel and pebble. 51 Chegan suite — Pg3— Pg} 1.5—191.8 m Gray clay with a slight greenish tinge and with rusty ferruginous spots, mica scales, pockets and interlayers of siltstone having fine lamellar structure when dry. There are interlayers of silty, slightly micaceous clays with a large amount of fine, carbonized plant residue, sparse inclusions of glauconite and pockets of quartz sand. 53 Talitsa guite —'Ps, 191.8—231.15 m Light gray, silty, slightly micaceous argillite, slightly gaizelike in some places with sparse imprints of fish scales and carbonized plant residue. A sample of gray silty clay of the Chegan suite from this well ata depth of 47.5—56. 3 m was examined. Because of the abundance of Pyxilla oligocaenica var. tenuis Jouse, the diatom complex was placed in the Early Oligocene (?). Together with remains of the diatom flora, a peculiar complex of silicoflagellates with 12 species, varieties and forms was found (Table 10). The table shows that the dominant silicoflagellates are Dictyocha elata var. media Gleserf. media etf. reducta Gleser and Distephanus antiquus Gleser. The latter species is represented mainly by pentagonal and hexagonal skeletons; heptagonal and octagonal shapes are less frequent. Dictyocha rotundata Jousé var. rotund- ata is encountered in considerable numbers; the remaining species are very rare or rare. Lozva River, near Pristan Samples from the well cores 26 (Tyn'inskii sector), 361 (Lozva sector), and 268 (South Lozva sector) were examined. The material from well 26 contained only unidentifiable diatom remains in a semidissolved state. Well 361, Lozva Sector, norrhor Fens pan Quaternary deposits 0.0—6.7m Loose loams with plant roots and subangular quartzite and porphyrite fragments. 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DIDISDY “ABA “72 °C ‘Z[NYOS «wou -1U *} DyD]NIIdY “JRA DYIUVIDIA] “| *10SO]1) (zjnyos) vunryspaduvyoav vyr0hj91q sotoads SOIL [[ASETJOOIIS ‘O19 ‘ds sitfdouvydag ‘ds supp “dg opizhg o1S8uozeq Ajqeqoid am Inq ‘poeuTWIe1ep aq 10U P[Nnoo YyoTYyM satnasnay paatosstp Ajired jo sasse PMITIBIV lo'yge—z'e9e| Sz auqBiy | 8¥E—S CVE] Ve J ‘asnor vI,UaI0an] nd D]JAIMNOUNA ¢ ‘unin vuafiwisvd *d ¢ ‘esnOf VII2D4N DIAYI0L3} G ‘unig, wnsoursfisijod snjnvjwazy “unain y purydasol "aed snjoajid viugvUIs J e ‘UNI 22SS2aM) UWNI7DLAIIA T € “UNI Ms4aqglay wn14D19914 J gels) S ‘IYG] SNpvauy snIsipou19s09 "3d -O2[ed ‘unIy) DIp ‘a1ins Aqreg S -auldajqul “ted si4ing sixfidounyday esuyeL| art@ry |O'SEE—SHEE] 22 S ‘unin, wnsourshsijod snjnviwapyy € ‘UNI $DsafqUI4VI YIAYIOLA} J “und G puiydasol “ieA snjoajid vI49vUIA T re ‘unInD 21SS2aM WNI7018924 J aug0 ‘UNI Dipausaju. “IBA 9 qo ‘unIny snupuijzAd “TRA sting “9 Sete g ‘sypey (‘AoIg) Tosaf srridouvydajg Aieg G “UNI 99119Q1S “IBA DIVIINS V.11S0]2 Wl 13g ‘o1ins eSIITeL so[nisny peaosstp Ajised pur sjuowsey Aueul yiIM eIoy padrasaid AyIO0d autissy |0°'S62—0'%62| 6F uon -en[eAo Ploy] satoads ot aATiel o8e + w01e 1p Fant ue ons ABoqoutT ‘wndod = oe. 1 Pp : q -wes soxatdulod WOleIp 9NsTIBIDeIeYD ,UPISTIg IPDU IBATY LAZOT UO [OE [TEM WoO sotduies jo stskteue dtdoososoIW Jo sNsoy “TT ATAV.L 55 56 11.3—31.0 m Sand and sandstone, analogous to above description; the lower part is richer in clay, having interlayers of dark gray silty clays, gravel and small pebbles of eruptive rocks. 31.0—43.7 m Fragments of gray, gaizelike argillites with a considerable amount of sandy material; in places the rocks are more monolithic, highly fractured and crushed. 43.7—68.7 m A bed of gray, silty, slightly gaizelike argillite with laminas and lenticles of a light gray, micaceous siltstone with dark gray, crumbled argillites and fine, slightly cemented sandstone with quartz gravel; the interlayer at the bottom of the interval is rich in gravel-pebble. 155.5—341.0 m Gray argillite of slight greenish tinge, gaizelike, greasy to the touch, with interlayers and lenticles of glauconitic sandstone and with quartz gravel and other eruptive rocks, breaking down into more or less parallel plates witha rough fracture surface; there are interlayers of dark gray argillite with small, carbonized and pyritized plant re- mains. At the top of the interval interlayers of sandstone are encountered similar to those described above; in the lower part there are laminas of silty argillites with numerous glauconite grains as well as fragments and interlayers of a brown, solid, finely granular siderite and of manganese ore. Slavgorod suite — Crg™°P 341.0—390.0 m Gray argillite with a greenish tinge, in some places greenish gray, with interlayers of lighter-colored varieties, slightly gaizelike. The rocks break down into rough, sharp-edged fragments. Underlain by white, kaolin clays. Results of the microscopic examinations of 13 samples from the well are shown in Table 11. In the range of 12.3 —217.3 m, traces of algae could be detected. Such fossils were found in only 2 samples from the Talitsa suite: no. 19, depth 292.0—295.0 m, and no. 22, depth 334.5—338.0 m. The diatom flora of these two samples are very close; however, certain differences were evident. Thus, at a depth of 334.5—338.0 m, Coscino- discus lineatus Ehr. dominates, and frustules of Triceratium heibergii Grun. are frequent; both of which do not occur in the over- lying sample. On the other hand, at a depth of 292.0—295.0 m there are numerous frustules of Melosira sulcata Grun. and Stephanopyxis ferox (Grev.), absent in the deeper sample. The diatom complex encountered in samples 19 and 22 is analogous to the Early Paleocene diatom complex described from the Serov and Ivdel areas. Complexes of both samples show both similarities to and differences from the lower and upper complexes of the Paleocene. With the lower complex, they share an abundance of Trinacria pileolus var. josephina Grun. and absence of Stephanopyxis lavrenkoi Jousé and Hemiaulus polymorphus var. frigida Grun. They have in 56 common with the upper complex large amounts of Stephanopyxis ferox (Grev.) Ralfs (sample 19) and Coscinodiscus lineatus Ehr. (sample 22). These features are apparently due to similar environmental conditions. On the basis of the taxonomic composition, the diatom and silicoflagellate floras can be placed in the Early Paleocene. The silicoflagellates are represented in both samples by a limited number of specimens belonging to several varieties and forms of Dictyo- cha triacantha Ehr. In addition, individual skeletons of D. archan- gelskiana (Schulz) Gleser and Mesocena aff. apiculata (Schulz) Defl. were encountered at a depth of 292.0—295.0 m. Well 268, Pristan settlement on Lozva River Quaternary deposits 0.0 —64.3 m Brownish gray clays with boulders, gravel, carbonized plant remains and fragments of argillites. Talitsa suite — Pg, 64.3 —80.3 m Dark gray, deformed argillite with numerous sliding surfaces, with laminas and lenticles of gray siltstone and light gray sandstone. Below the middle of the interval the argillite gradually merges with fine, micaceous, light gray sandstone. Carbonized plant remains are present. 80.3 —83.8 m Slightly calcareous clay in places. Slavgorod suite — Cr§o-stcP 83.8—164.1 m Greenish gray argillite, slightly gaizelike in places, with aggregates of a light gray micaceous siltstone, breaking down into more or less regular plates at an angle of 10—12°. Below 146.4 m the argillite becomes more monolithic, in places strongly silty with accumu- lations of carbonized plant remains. Below 157.0 m the rocks merge gradually into a gray, greasy argillite with interlayers of dense, gray, slightly micaceous argil- laceous siltstone. Underlain by continental deposits of the Lower Cretaceous. Seven samples were examined from the well core. The sample from the Talitsa suite (depth 64.3— 80.3 m, top) contained no diatoms, as did samples from the lower part of the Slavgorod suite (no. 13, 146.6— 150.4 m; no. 15, 157.5—164.1 m). Diatoms and silicoflagellates were encountered in 4 samples from the Slavgorod suite (nos. 8, 9, 10, 12) in the range of 83.8—136.2 m (Table 12). 57 57 mmumOoN-N woos <4 uoTti -enyeAd aATIeI -1quenb *Z[NYIS DIVIPDL-2}D] “J VIVjNIIdD “IRA “2 *G ‘pypjnjidp “| “Wwe pivjnjidv "eA DYIUDIDIAZ DYI0h}I21q ‘Ted vuafiajnov vnusog ‘euuey], rajydwis °*7 ‘euuRey], v7nounf vjnwoshT ‘1ase[y Bynprwinz, “4 “euUue_, 1207404 071990]]04 *Z[NYIS vypINfI47 DNULOD ‘euuRy, =raydwis “7 ‘euueR], vynaun{ vpnwoishT “euURF{, «22U0710Y 07419902104 satoads SOI [[ISETJOOTIS -uedure9 -uetuolues -uedwired -urTuolUes sr ses Lo ttt oD OD SH J c G V Vy i if G t+ © uot] -enpTeAa dATIPI -TquUeNnb ‘asnor suvsajza-pid “HY ‘unig §=wnsourshosijod snjnviway ‘gsnog 21z7NYyIs Wn17DL9914 [ ‘asnof S271QDLIW 14279L0g ‘Z[NYIS SnNuossip snasypoursso0) ‘asnOf va9D}]a19 “IRA yo 11z7NYIS “IBA “UTOJS 22z7NYIS “Gg ‘asnor snnbijyup sitidounydays ‘UND vIIAgGIS “TRA *s ‘| do-3s-uo ‘unin Divjnuala “AWA DzIVIINS DALISO]A LY ‘AOJOIY aWs0Uua DWWDAZOJOUNT ‘(squowi8ey) esnof vaIv}019 vP,Izig ‘asnof avaouissiUD visIDUIL I ‘asnor suvsaja-pid "7 ‘unig wnsourjshofijod * 7] ‘asnor s7j7spaf snjnviway ‘gsnof SI71QDugW DIYZIAL10g “Z[NYIS SNUOSSIp SNISIP0UIISO) ‘asnof vaID}a19 “IRA qo MzjpnyIs “IBA "ULES Mz7NYIs *¢ | dod-1s-u9 ‘unIy) Dipau -13]U1 “IRA Siuanz sixfidouvnydajg satoads saxatdWiod WOIeIp ITIstI91IOPIeYD ‘olins Ppo1OSAeIS z415 ‘o2mns POJOSARTS ase pue o1ins aSuli Yst -ud018 & yam att -[18ie Kein |g" 6 arp ere Ae | atppru ystueeaID |')'88—-8'E8, 8 ASojouay aid -wes URISTIg IRAU IOATY PAZOT BI UO ggz [TOM WoOY soatdures Jo stsXkteue otdoosoiotw jo synsoy “Zl AIGVL 58 58 _— wom MaAA uoli -en[eAd dA1121 -Tjuenb “Z[NYIS DIVIPV1-2]V] “| DIDJNIIdD “IBA “7 *G ‘pypjnaidp "y “WulaT DIDjNIIdD “IBA DYWUDIDIAZ DYIOAII1G ‘euuey{, raydwis *7 ‘euueyT vpnIunf vjpnwoshT “1ase[y) DjNpiwnz “4 “VUURL{ 2707404 0j1290]]0 4 ‘euuey, vpnoain{f vjpnwoshT “BUURTT 27U0210Y 0199D]]04 satoads SOIL[[IBLTJOOT|IS uel -urdwes -uPTUOIUPS uvI -ueduie) -ueTUOIURS uvT -urduird -uPTuoIURes Nw Idd N19 u st ‘asnof vaanja19 v1712Aig ‘asnor supdaja-pad “PT ‘unig = wnsouljshoijod snjnorwayy ‘asnOf apAOWIssiUD DI149DUI4 J ‘Z[NYIG snuossip snIs2zpour9s0) ‘UNI, DIpawsaju1 “IRA sting “9 ‘9SNOf DIID}A1I “ABA 4d 1zjnyos ‘ABA “UldIG wWznNYyIs *¢S ‘asnor snnbijuv sixfidounydajg “UNIN) DIILAGIS “IBA "Ss “ “und 01180] JA DID]NUaLI “IBA DIDIINS pa0vjJa19 0771zhg ‘gsnof 21Z27nYyIs wnI7D419914 J ‘Vzynyss "JeA gsnof 2227NYIs “9 ‘asnor snnbijuv sixidounydaz9 ‘UNID DI1LAQIS “IBA ‘*S * “unIy 04118013 Jy ‘asnor DIDjNUaLI “IVA DvIINS ‘asnof vaIvj}019 DIpIThg ‘UNIN) DIIUDP “TRA ‘0 “4H *D]]aq7UOpo “MWA “IYO D72A7UOpO wWnIIaYj01U0y PIOTJ wo1eIp jo any @ATIe -tuenb soroads soxojd Wo WoIeIp ITIsTIDIDeIeYD a8uti Yst do 4s-u0"D -U9918 & ‘ous YIM ait Z'98F poso8arts} - Is1ekery | —9CEV | Ch asuti yst eee -u9018 & ‘arms yam oat] r'e0I pososarys |} -pt8ieke1y | —9'00) | OF asut yst ey -usei8 do-3s-uo 79 aay ‘oums WIM aut -1183e Ae1N [g'g6—-0'88] 6 pososarts ase uw ae ue oimn ABOVENAT ‘yada ds pur ain mded | ues (panutuod) ZL AISVL 59 59 Three samples (nos. 8, 9 and 12) revealed well preserved remains of abundant diatom floras of almost identical composition, differing only with respect to the numbers of some species. All the samples were rich in valves of Stephanopyxis schulzii Stein. var. schulzii et var. cretacea Jousé, Coscinodiscus dissonus Schulz and Pyxilla cretacea Jousé. The valves of Poretzkia mirabilis Jousé, Hemiaulus fragilis Jousé, Trinacria anissimovae Jousé and Eunotogramma enorme Krotov were present in smaller amounts and in some preparations only. Sample 10 contained a poorer complex. A similar flora found on the eastern slope of the Urals has been placed in the Santonian-Campanian. Numerous skeletons of a few silicoflagellate forms were found together with the diatom frustules. Sample 10, however, contained very rare skeletons of only 2 silicoflagellate species. A total of 8 silicoflagellate species and varieties were encountered. Most abundant are the silicoflagellates of the families Vallacertaceae Defl. and Cornuaceae Gem. Vallacerta hortonii Hanna is abundant in all the samples. Lyramula furcula Hanna is also present in all the samples, being abundant in sample 10 and frequent in the rest. L. simplex Hanna is relatively scarce in the entire section. Samples 9 and 12 contain single skeletons of Vallacerta tumidula Gleser. Species of Cornua Schulz have a very limited distribution. Skeletons of silicoflagellates belonging to the family Dictyochaceae Lemm. (Dictyocha triacantha var. apiculata Lemm. f. apicu-= lata etf. lateradiata Schulz) were encountered only in 2 samples in very small amounts. These slight differences in the qualitative and quantitative composition of the algal complexes of the examined samples do not make possible conclusions concerning a trend in the evolution of the silicoflagellate flora during the Santonian- Campanian. Area of the town of Ivdel Samples from wells 100, 130 and 564 were examined. Fossils of algae were found in a number of samples from wells 130 and 564. Well 130, sowth: of) fyvdel Quaternary deposits 0.0—12.5 m Brown peat on top is underlain by heterogeneous sand with pebbles, boulders and carbonized plant remains. 5698 60 Chegan suite — Pg3— Pg} 12.5—17.7 m Gray, greenish-tinged, greasy clays of finely stratified structure with lenticles and laminas of gray siltstone. * Irbit suite — Pg33 17.7—144.0 m The clays merge gradually downward into light gray argillites with a slight greenish tinge. Gaizelike, micaceous argillites with lenticles of micaceous siltstone and pockets of pyrite break down into more or less parallel plates with interlayers of argillaceous diatomites and a light gray, dense gaize. The argillites are under- lain by light gray, loose, slightly micaceous, easily soiled diatomites which split into irregular plates witha rough fracture plane. The diatomites contain laminas of glauconite-quartz siltstone of micaceous nature and scattered plant remains and shell imprints. In places the diatomite is richer in siltstone; downward it becomes denser and more argillaceous, and gradually merges into an argillaceous gaize. Serov suite — Pgi 144.0—168.0 m Gray to dark gray argillaceous gaize with sparse prisypki** of micaceous siltstone of subconchoidal fracture, splits into parallel plates with a smooth surface. There are worm trails, rare imprints of pelecypod shells, inclusions of plant residue, and len- ticles of a micaceous, glauconite-quartz sand. The gaize is underlain by a greenish gray clay with gravel, pebbles and interlayers of sandy clay containing a gravel-pebble material and siderite interlayers. Talitsa suite — Pg, 168.0—294.0 m Muddy gray, greasy argillite of lamellar structure, gaizelike in some places, splitting into regular parallel plates with micaceous, silty, often glauconitic material on the planes of lamination which are vaguely horizontal; pyritized plant remains, sparse shell fragments and fish scales are encountered. There are interlayers of eroded gravelite composed of fragments of quartz, siderite and other rocks. 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There is a gradual transition to the rocks of the Kuznetsovo suite. ° t Kuznetsovo suite — Cr, 319.0—325.3 m Laminated gray argillite, silty in some places, splitting into parallel plates with a poorly defined horizontal lamination. Downward the argillite becomes dark gray, laminated and greasy to the touch. The Kuznetsovo suite lies under a crust of debris. In the 26 samples from well 130 examined microscopically, large numbers of fossil algae were found only in the samples from the Irbit and Chegan suites (Table 13); those from the Talitsa, Slavgorod and Kuznetsovo suites did not contain remains of frustules and therefore do not appear in the table. Two diatom complexes are evident in the Irbit suite. The older of these complexes is rich in only 2 species of the genus Coscinodiscus (C. moelleri var. macroporus Grun. and C.uralensis Jousé) that are characteristic of the Middle (?) Eocene. This Middle (?) Eocene complex was found at a depth of 137.3 m (sample 33), 128.7 m (sample 31) and 116.0 —120.6 m (sample 29) in gray argillaceous diatomites. Above (at a depth of 106.0 m) the number of Coscinodiscus uralensis Jousé frustules become rare, while C. moelleri var. mac roporus Grun. becomes abundant. The younger complex of the Irbit suite is characterized by the following features. Considerable amounts of Coscinodiscus Ehr. species are encountered, suchas C. argus Ehr., C.decrescens var. polaris Grun., C. decrescenoides Jousé, C. moelleri var. macroporus Grun., C. payeri Grun., C. radiatus Ehr., as wellas Stephano- pyxrs_ednta Jousé, S. punctata Jousé, Triceratium exornatum Grev., Trinacria exculpta (Heib.) Hust., etc. The systematic composition and quantitative development of different species of the diatom complex varies to some extent with depth, but its general character remains essentially the same from 38.7 m to 91.2 m. A similar diatom flora on the eastern slope of the Urals and in the West Siberian plain has been placed in the Late Eocene. The light gray argillites from a depth of 31.8 m (sample 11), 29.0 m (sample 10) and 17.7— 24.7 m (sample 9) contain valves of many typical Late Eocene species. Usually these are not numerous, but occasionally they may be rather abundant (Stephanopyxis punctata Jousé ata depth of 31.8 m and Coscinodiscus moelleri var. macroporus Grun. at a depth of 29.0 m). Very often, but not in all the samples, this stratum contains valves of Pyxilla gracilis Temp. et Forti. A similar flora on the eastern slope of the Urals is regarded as transitional from the Late Eocene to the Early Oligocene, and is placed in the Late Eocene (Krotov and Shibkova, 1961). 71 72 A usual feature of the complex from the gray, greenish-tinged clays of the Chegan suite at depths of 16.5—17.7 m (sample 8) and 16.0 m (sample7) is the abundance of Pyxilla gracilis Temp. et Forti and the presence of numerous P. cf. asiatica Jousé. Other typical diatoms of this com- plex are Coscinodiscus decrescens Grun., C.argus Enhr., C. mirabilis Jousé, Stephanopyxis megapora Grun., Bright- wellia hyperborea Grun. Sucha flora might be placed with reserve in the Late Eocene— Early Oligocene. The literature does not indicate the abundant occurrence of Thalassiosira aff. zabelinae Jousé in the uppermost sample (depth 16.0 m) and the presence of very rare valves of Pinnularia antiqua Tscherem in the 16.5—17.7-m interval. Changes in the diatom flora were very gradual during the Middle (7?) and Late Eocene, as well as from the Late Eocene to the Early (?) Oligocene; the boundaries between the respective floras are arbitrary. The silicoflagellate flora of the Middle (?) Eocene is poor, both quanti- tatively and qualitatively (Table 13). Of the 7 species, varieties and forms of silicoflagellates examined, all are represented very rarely, except for Dictyocha frenguelli var. carentis Gleserf.carentis, whichis frequent at a depth of 137.3 and 128.7 m, and the rare occurrence of Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata at a depth of 106.0 m. In the Late Eocene, in addition to the forms included in the above Middle Eocene flora, a whole series of new silicoflagellates are encountered — varieties of Dictyocha deflandrei Freng., D. frenguellii Defl. var. frenguellii, D. frenguetlliivar. ecarentis f. incerta'Gleser, D. rotund ata Fousé var.*rotundata.D. tr ansitoria pels D: dibula Ebr. var. fibwia f.itabuda Sete. Some Late Eocene forms become very numerous: D. frenguelli var. carentis f.incerta Gleser, D. deflandrei var. completa Gleser f.completa, D. rotundata Jousé var. rotundata, D.triacantha var. apiculata f. minor Schulz, D.transitoria Defl., and some varieties of Naviculopsis biapiculata (Lemm.) Freng. These forms are not abundant in all the samples. The composition of the silicoflagellate flora changes upward (Figure 2). Thus, from skeletons of D. rotundata Jousé var. rotundata begin to appear from a depth of 86.7—91.2 m, D. deflandrei var. completa Gleserf. completa from 74.5 m, and D. transitoria Defl. from 55.0—60.4 m. Skeletons of D. deflandrei var. bicornuta Gleser are first encountered ata depth of 31.8 m, and D. obliqua Gleser in the 17.7—24.7 m interval. In Late Eocene — Early (?) Oligocene deposits (depth 16.5—17.7 and 16.0 m), some of these species (D. deflandrei var. bicornuta Gleser, D. deflandrei var. completa Gleser f. completa and f. producta Gleser, D. rotundata Jousé var. rotundata) occur in considerable amounts. Judging from the material from well 130, there was no sharp difference in the taxonomic composition of the Late Eocene and Late Eocene — Early Oligocene (?) silicoflagellate floras. Nearly all the species found in the Late Eocene diatomite stratum are also encountered in the uppermost part of the well. Moreover, there are hardly any new floral elements in the Late Eocene — Early Oligocene (?) except for very rare skeletons of D. fibula var. fibula f. rhombica Schulz and Mesocena circulus Ehr. 72 (2)aus008 110 Ayieg —9ua004 21e] dua00d aua00g 2187] (¢)arpptwi snjnguia buazosay sna -)yapydsiway snj}douun9 JOU IDA 0)0)N91d029 s1sdo)NIIADY D}0)N210D19 “sDA pyo)naId019 $18d0)NIIADN Joulwy S}wsaU? JDA Dy}uD901.43 DYy20h}a) DJD}SOY wDA Dy3UDIDI4} DYIOA}IIE JouIw y D2DjN21d0 YODA DYIUDIDIGZ DYIOA}IIG pjp)n2dD°4 St DA DY}UDIDI} a at Aisne nee bela moan coped Ts pwopisuds} DYyIOh}IIT 4 osounds py20h}20¢ — ike 3 eee "4 D}Dpunjos ‘UDA Djopunjos DyI0h}I1¢G * pnb1)90 py20h}21g DJasijawd)} ‘UDA Duajuyjawo} pauee| | Djvagu? J $ijuas0I wpa manbuasy DyI0h}01G CO yp smarty ora (I || | lel LL TL LT Bojuad von ons owoha| AL UT | TE TT TT von onary oyooriong| Kt [IT | Tit | Ut Ty tT p2luaDI0a ‘4 NNGUUDA 0)NQ?4 DyD0h22IG DINg7y J 01NQIY ‘UDA p2Ngiy oYy20h}20g D}DJa‘JDA D}D}a DYIOh}IIG pjanpoudj DJa)dwoa DA laJpub) jap Dy20h}2I¢g D}a)dwo2'}0}a,dwo7sDA lavpunz jap py20h}01¢g DJNUJOIIQ “IDA laspub) yap Dy20h}21¢g $1JU9IDI*J $1]UaIDI up npjanbuas DYyI0h}I1G hee i Wilt 3 ny Ml lr MoM ul I ; "oil ll y" Mi uy | ile | a[yoid d1Z0ToyIT peUululexa sojduies Joon : 73 Distribution of silicoflagellate skeletors in rocks of the Irbit and Chegan suites of the Ivdel area (well 130). x 1,000; FIGURE 2. 1—sandstone; 2—sand; 3—clays; 4 —argillite; 5 — gaizelike argillite; 6—marl; 7 —diatomite; 8 —gaize; 9 — brown peat. Well isib4 a inroerth voreived en Serov suite — Pg} 0.0—50.4 m Loose, light-weight diatomite, whitish yellow above, light gray below, with interlayers of denser diatomite. Stratification vaguely horizontal. In some places ferru- ginization and rare worm trails. 50.4—74.0 m Light gray, fine grained, slightly micaceous sandstone with sparse grains of glauconite and lenticles and interlayers of diatomite reaching a thickness of 40 cm. Isolated fish scales, rare carbonized vegetation residue. Gradual transition from diatomites to sandstones. 74.0—82.5 m White, sometimes quite sandy diatomite. Slight ferru- ginization; interlayers of sandstone, as described above, in some places. 82.5—98.0 m Gray and bluish gray dense gaize, breaking down into unequal, sharp-edged fragments. The gaize is greatly enriched in silty and argillaceous material and contains rare carbonized plant remains and localized accumula- tions of carbonate rocks, rare grains of glauconite. Sparse gravel and a considerable amount of pebbles of eruptive rocks are located at the bottom of the interval. Talitsa suite — Pg, 98.0—233.0 m Gray laminar argillite, in some places dark gray, with monolithic sectors, greasy to the touch, gaizelike toa various extent; the argillite breaks down to parallel plates with a rough fracture plane. Rare lenticular masses of fine gravel and glauconite. Stratification vaguely horizontal, in some areas clearly so. Rare carbonized vegetation residues. 233.0—236.0 m_ Light gray to white, greenish gray, in some places strongly argillaceous sandstone with interlayers and lenticles of green silty clays. Numerous grains of glauconite, siderite, gravel and fine pebbles. Slavgorod suite — Crs" "oP 236.0—261.8 m Gray to dark gray, greenish-tinged, greasy, slightly micaceous, laminar argillite, breaking down to more or less parallel plates with a rough, often knobby fracture plane. Sparse scales of mica and carbonized vegetation residue on the laminar planes. Stratification of the rocks is poorly defined, in some places it is vaguely horizontal. Rare imprints of invertebrates. A total of 18 samples from well 564 were examined. Algal remains were found in samples from the Serov suite from a depth of 4.3 —75.5 m 74 (73) auac0q Ajieg ausd0eateg Arie Dysngou sisdo)naiaoy D}D)NI}0D1q “IDA D201n910D19 sisdopnaIADN JOUIW *f S}WdaU) “DA pDyjuons0I} DYI0h}IIG SIWsaU):J SlWsaU) “IDA pyjuo901} DyI0h}21g D}D}SDY IDA Dy}uDIDIJ} DYI0A}2Ig JOUIW J D}D)NI}dD “IDA pyjupgni4} oyrohj20g D}D)NI}0DY 0JD]NIID IDA pyjupo01J} pyI0h}21¢g DYy)]UDIDId} Jy DYJUDIDIS} IDA vyjuoanIJ} Dys0hj2I¢g oynayAbu Dya0h}01G D}I2J}SU0I “UDA duasijawD) Dy20h}0I1¢g DuaJi]awd) ‘JDA puasnjawD) by2ohj01g Do)uap20a°J DIngyJDA ppNgQIy DyaoA}IIG [a] 7 Feed 8 i p}p4u0ja nya0h}21¢ pupixsjabupyaub ny20hj21¢ rajdws opnwosh7 p)nauny v)nwDsA7 NUOIJOY 0}JaID])D/ aipepogone Pein aH | UL SER: SOHO R ROL clo 2 $$ 116 12 13 14 FIGURE 3. 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The flora was most abundant and well preserved at a depth of 172.7 and 208.0 m in the Talitsa suite. Unidentifiable, semidissolved frustules were encountered in varying amounts in the lower parts of the section. The diatom frustules were in a particularly poor condition at a depth of 230.5 and 233.4 m. No evidence of algae was found in the upper part of the Talitsa suite (109.6 and 147.7 m); on the other hand, the lower part (234.7 m) contained a fairly rich diatom complex. The complex of the Talitsa suite of well 564 is characterized by the abundance of Stephanopyxis ferox (Grev.) Ralfs, S. turris var. intermedia Grun., and in some samples S. lavrenkoi Jousé, Trinacria pileolus var. josephina Grun., T. pileolus Ehr. var. pileolus, Hemiaulus polycystinorum Grun., H. poly- morphus var. frigida Grun., Melosira sulcata var. siberica Grun. or var. biseriata Grun., Triceratium weissii Witt., Goniothecium odontella Ehr. var. odontella. Analysis of the complex and comparison with published data show that the complex is qualitatively and quantitatively analogous to the described Early Paleocene diatom flora of the eastern slope of the Urals. However, it was impossible to distinguish between a lower and an upper complex as established by Krotov (1957a) and Krotov and Shibkova (1961). As can be seen in Table 14, the silicoflagellate complex of the Talitsa suite consists mainly of varieties and forms of Dictyocha triacantha Ehr.; other species of the family Dictyochaceae Lemm. are D. archangel - skiana (Schulz) Gleser and Mesocena aff. apiculata (Schulz) Defl. The family Vallacertaceae Defl. is representedby Vallacerta hortonii Hanna, Lyramula furcula Hanna, L. simplex Hanna. The amount of silicoflagellate skeletons increases gradually upward in the section. Very rare skeletons of 4 varieties have been found at a depth of 219.5 m; at a depth of 208.0 m there is a slight increase in the number of skeletons of Dictyocha triacantha var. hastata Lemm. and D. triacantha var. apiculata f. minor Schulz. At 172.7 m, D. triacantha var. hastata Lemm. and D.triacantha var. inermis f. minor Gleser become dominant; finally, D. triacantha var. hastata Lemm. and D. triacantha var. inermis f. minor Gleser are dominant in the uppermost sample containing silicoflagellates. Mesocena aff. apicu- lata (Schulz) Defl. is rare. Remains of a rich and well preserved diatom flora were found in all the samples of the white diatomites of the Serov suite (Table 14). The Serov suite samples of well 564 are fairly uniform, despite some slight fluctua- tions in the frequency and species composition. The abundance of Melo- sira sulcata var. siberica Grun., Stephanopyxis turris var. 86 intermedia Grun., Triceratium kinkeri A.S., T. mirabile Jousé, T. ventriculosum A.S., etc. is reminiscent of the Early Eocene flora of the eastern slope of the Urals; on these grounds, the flora encountered can be placed in the Early Eocene. However, some characteristic features must be mentioned, such as the presence of Coscinodiscus sp. (C. aff. moronensis (Grev.) Rattr. as deter- mined by Anisimova), C. lineatus Ehr. and Pseudostictodiscus angulatus Grun. in the dominant complex. In addition, small amounts 81 80 of Grunowiella gemmata (Grun.) V.H. occur in the upper part of the suite. These features apparently are due to some local ecological fac- tors. Thus, on the basis of diatom flora, the examined diatomite stratum can be placed in the Early Eocene. The Early Eocene diatom complex is accompanied by remains of a characteristic silicoflagellate flora numbering 12 species, varieties and forms, all of the family Dictyochaceae Lemm. Most of these silico- flagellates do not occur in the samples from the Talitsa suite. The skeletons of Dictyocha lamellifera var. constricta Gleser and D. fibula var. fibula f. eocaenica Krotov predominate in all the samples. D.lamellifera Gleser var.lamellifera is represented by a considerable number of specimens in some samples, while D. navicula Ehr. and Naviculopsis robusta Defl. appear in all the samples at a low frequency. Very rare skeletons of Dictyocha elongata Gleser were found only in the lower part of the suite, and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata appears to be confined to the upper part. The silicoflagellates occurring in both the Talitsa and Serov suites (Dictyocha archangelskiana (Schulz) Gleser, varieties and forms of D. triacantha Ehr.) are represented in the Serov suite by isolated specimens in some samples only. Only skeletons of D.triacantha Ehr. var. triacantha f.triacantha are rare at a depth of 18.0m (sample 2). Serov area Samples of 3 wells (459, 762, 771) were examined from this area west of the town of Serov (from the collection of D. V. Osadchei, 1956). Well 459 Quaternary deposits 0.0—26.0 m Peat overlying fine sand with fragments of decayed wood. Irbit suite — Pg3-3 26.0—45.0 m White, light, very easily soiled diatomite, crumbling into irregular fragments, becomes downward more argilla- ceous, light gray, denser, heavier and greasy. The diatomite splits into parallel plates with an irregular plane of fracture. 82 Serov suite — Pg} 45.0—48.0 m Gray to dark gray gaize, splitting into parallel plates with sharp edges, sometimes with a subconchoidal fracture. The slightly micaceous rock resounds upon impact and merges gradually with underlying light gray, fine- grained, firmly cemented sandstone. Talitsa suite — Pg, 48.0—84.2 m Dark gray, micaceous argillite in places slightly gaize- like, with pockets and interlayers of a fine siltstone and scattered grains of pyrite. Downward the rock becomes lighter-colored. 84.2—153.6 m_ Silty gray argillite with a very slight greenish tinge. The argillite is slightly micaceous, greasy, somewhat gaizelike with inclusions and interlayers of quartz sand, mica and fine plant detritus. 153.6—153.8 m Fragments of manganese ore. 153.8—163.0 m Quartzy-glauconitic medium-grained sandstone with isolated, rough pebbles overlaying light gray, fine- grained sand. Eight samples from the Talitsa and Irbit suites of well 459 were examined microscopically. The samples from the lower (144.5 m) and upper part (79.5, 66.3 and 52.4 m) of the Talitsa suite proved barren; algal remains were found only at a depth of 92.5 m. Because of the abundance of frustules of Stephanopyxis turris var. cylindrus Grun. et var.intermedia Grun., Hemiaulus polycystinorum Grun., Trinacria prleolus. Ehr. var.cpifeolus et var. josephina Grun. andthepoorer development of Stephanopyxis ferox (Grev.) Ralfs and Hemiaulus polymorphus var.frigida Grun., the diatom complex of the Talitsa suite (Table 15) resembles the lower complex of the Early Paleocene of the eastern slope of the Urals, but mainly differs in the greater amount of Coscinodiscus lineatus Ehr. The sample contains rare specimens of Mesocena aff. apiculata (Schulz) Defl., and very rare numbers of Dictyocha triacantha Ehr., D. archangelskiana (Schulz) Gleser and Lyramula simplex Hanna. All three samples examined from the Irbit suite contain abundant and well preserved fossils of diatoms and silicoflagellates (Table 15). Floristically, the complexes of all 3 samples are very similar; charac- teristic of all is the group of forms of Melosira sulcata (Ehr.) Ktz., Stephanopyxis turris var.intermedia Grun., S. broschii Grun., Coscinodiscus moelleri var. macroporus Grun., C.uralensis Jousé, Goniothecium odontella Ehr. var. odon- tella, Hemiaulus polymorphus var.frigida Grun. and Grunowiella gemmata (Grun.) V.H. (the latter species was not found in the deepest sample). A similar diatom flora west of the West Siberian plain is placed conditionally in the Middle Eocene. 83 (81) on “= om = =—NW uon -eny[ead aanel -lquenb ‘pypjnaidp "y ‘WUWd'T D7D)NIIdD “IRA DYIJUDIDIAZ “(7 ‘piafiy -]9WD] “IVA IASI) viafipjawn}, *q ‘s1qUadDd *} JOS 0] syjuaipo “TRA 1npjansuas{ *q ‘pynqut *y pyngrf “aeA “ay vyNngrf vyI0hz21q ‘Tod visngos “Ay ‘Taso (z[NYoS) sowrw “TRA “Q “AY ‘pypjnaidpig “IeA “Buddy (wwe) vzp7n21dn1q sisdopno1avAy “sr -daur "J “WWOT siwiour “IRA “7 °C “WOT DIDISDY “IBA “7 °G ‘pyvjnoidp “yj “mwa D7D)NIIdD “IVA DYJUDIDIA] “(J ‘IQ vynaavu *q ‘pd afiy ~]2WD] “IBA JBSO]X) V4afipjawn) *(] ‘s1quadDo *y Toso] syuaipo “IRA IM1ppansuad{ °C ‘pyngif *y vyngif awa “aya v7ngif ‘ “lose[y) VyDSu0j,a YYyI0h}21q satoads SOILT[IBEYOOTIS ou9a5 -0g (2) OTPPIIN euaf -om (2) STPPIW RIOT wo1eIp jo a8y ws wD wn ww N © suo w OD uD OD LD io) uon -enpeaa aATIe2 -luenb ‘unin opie -f ‘rea snydsowfhjod snjnviway ‘asnof sisuaypun +9 ‘unin sniodod -IDUL “IRA 14a]]90W snosipoUlIzseD UNIX) DIpsuwazUl “IBA Siding “9 ‘unin 1y2s04q sixidouvydags *(suJOJ Jo dnoi8) *zyy (‘ayq) 27v97NS D«IsOjapy "HA (Cunsy) vjpwwas pjjaimnounsy 2] a7U0po ‘IBA ‘IY Y7Ja7UOpO wni92aY201U0y ‘qlay] purses visopUuid J ‘unl vps -14f ‘eA snydiowfjod snjnviwayy ‘asnor (‘1yq) 0707 -uapid? “IRA ihawon, viydjnppig ‘asnor Sisua]D4n * 9 ‘unIn) snuod -04IDUL “IBA 142]]20U SndSipoU1Is0) ‘Vly Cpsouids §=paisoyro0u J ‘UNI vIpamsaqur “TRA siding *g ‘unigy 1y29S04q sixidouvyda,s *(SuIOJ Jo dnox8) *Z7M (‘1yq) 27vI7NS varsojapy satoads saxotd wos woletp dNstIaIORIeYD Poe AOIAS ‘ECP [OM WoO satduies Jo UONeUTUIeXa SIdooSOIOIUI Jo SITNSey “CL AIGVL 84 ‘Simms 11qJ] a1Tw01e I e-gdd Sayer qi] a1woleid age A8o0jouqy] pure 91mns Tou Cadtc 84 (82) uot} -enTeAd ATIEI -Tuenb od (zjnyog) vynynaidn “yye buithodeg “JOSO[H) 4OUIW "} STU4aUI “BA ‘7 “CQ “Su dau “y “WWATY S7wdaur “IRA “7 “(7 ‘WUT DDISDY “ABA “] “(7 “‘z[NYyoS Louru ‘J pyvynaidy "1eA vYyJUvIVIA, = *(T *"1aso]D (2jnyos) vuvrysjasunyoun vYysoh}21(T “euuRp] vaydwis vynwoshT ‘pyopnaidpig “IRA “BUdIY (‘wutoy) vyvjnoidniq sisdojna10v Ny “WUE DIDISDY “IVA “2 “(T “ZNYIS Lourw ‘IRA DYyJUDIDIA? §*(T ‘pial -1]]@WD)] “IBA JOSopH v4afij_JawD) *(T ‘SiqUadDd “} LOS ‘IeA lpjansuadf{ *C ‘png *J pynqif “aka “ayy vynqif vysohjo1(7 ‘| pyojnaidv -d3[9 $1]UALDI ‘pyojnaidvig “IRA “BUdIg (wwe) v7p)nI1dv1q sisdojnoiaD NJ ‘WWoT Dypispy “eA ‘7 * *Z[ NYS dou "y vyojynaidv ‘reds "7 “C au99d -02[ed Aqied 9u9090 -o¥ (2) aT PPI Quo0 -og (2) ATPPIIN oA N 21 tL uw i *p112qU0po ‘RA ‘IY VPaIUOpo wnII0Yj101U0L) ‘gsnofr 27 pruyas snosipoyjuvI py ‘ana vurydasol ‘rea ‘d ‘J *sn]0a] -ad ‘eA ‘IU snjoazid vidopur ‘unsy vpisidf ‘rea snydsowhjod * 7] ‘unin, wniounshohjod snjnviwa fy ‘IY SNypaury snosipourssog ‘UNI, DIpamiaqur “IeA “7 *S) ‘unr smupuryho "“TeA Siinz *S) ‘sypey (‘AorN) rodaf sixidouvydary *D)]]aqUOpo ‘eA “IY DIJaUOpo wn219aY201U0H ‘undny) opis -f “aed snydsowhjod snynviuca yy ‘asnor sisuayvun *O ‘ung snsodos pul ‘IBA IMapjaow sngIsipoUu19so0) ‘UNI DipamsaqUr “IBA S14dNp *G ‘unig 11yo2souq sizhdouvydas *(SuIO} JO dnoi8) ‘zy (Ay) 07097NS v«ISO;apy ‘HA (uns) pypwwad vpjaimounsy ‘asnos S478 04 "IRA DdaflUI4DI VIAYI0L I}. D1] a1U0po ‘IBA “AY VPJaUOpO wn19aY4,01U0H -10dn9 183d ‘Q1Ins eSIITe.L z e-aed ‘oltns qi] z g-aed ‘aiins 1143] a1tu01e 1d a1TWI0 11 TT IB1V oc oF satoads $O1V[ [ase YOOTIS v10yy wo1etp jo any uoll -enteAd daniel -ljuenb satoods soxo[dwod WOoIeIp TIsTIAIDeIeYO ase pure aiIns ‘ou aid -wes ul ASojoyl TUT | ndag (ponutquoo) St ATaVL 85 There are 12 species, varieties and forms of silicoflagellates. Dictyocha frenguelli var. carentis Gleserf.carentis is numerically predominant in 2 samples. While frequent in the upper sample, D. triacantha var. hastata Lemm. and D. lamellifera Gleser var. lamellifera are rare or very rare in the lower strata. Skeletons of D. fibula Ehr. var. fibula f. fibula are frequent at a depth of 38.0 m, and rare in the other two samples. All the other forms are very rare or rare. Skeletons of D. elongata Gleser, D. triacan- tha-var.inermis Lemm.frinermis, Naviculopsis robasta Defl., N. biapiculata var. minor (Schulz) Gleser, not found in deeper samples, were encountered at 35 m. Thus, well 459 reveals the presence of 2 silicoflagellate complexes, one from the Middle (?) Eocene, the other from the Early Paleocene. Well 762°) Zamaratskii sector Irbit suite — Pg3-3 0.0—9.0 m White diatomite, yellow-tinged with spots of ferrugination, light, loose and easily soiled with fine oolites of iron, rare quartzy gravel, and silty material in places. Serov suite — Pg} 9.0—35.0 m Light gray, very slightly micaceous, light, easily soiled diatomite, loose above with fine silty and sandy material of somewhat darker color due to carbonized plant residue. 35.0—40.2 m__ Light gray (dark gray in some parts), slightly micaceous, dense, solid gaize, somewhat heavier than the above diatomites, with pockets and laminae of siltstone and fine- grained sandy material, with conchoidal fracture. The gaize is denser with a large amount of sandy material at the bottom of the interval. Talitsa suite — Pg, 40.2—85.0 m Gray, micaceous argillite, in places slightly gaizelike, with interlayers and pockets of siltstone and sandy material with glauconite. The rock breaks readily into more or less parallel plates with an irregular plane of fracture; there are laminated argillites in places. Lamination is poorly defined. Rare inclusions of quartz gravel, grains of black earthy pyrite and large amounts of plant residue are encountered. 86 (84) uoT} -en[eAd aAT1e1 -tuenb ‘YJOd vIsngot “AJ ‘Josey (zjpnyos) sou "IRA DID]NIIdD1q sisdoj]NI1AaAv AJ “WUT DIDISDY “IBA "} “CT *S1u -aul “J “WUWAT Siuwsaul “LRA “7 ‘°C ‘Z[NYIS Lourw ‘IVA DYJUDIDIA, “(7 “IU VpyNIIevu “(7 ‘IdSO[D) DIDISDY “ABA “] “T “IOSO[) DIIIZSUOI “IBA *] “(T ‘pial -1]]9WD)] “IBA JOSO[H) D4afi1pJawv] (7 *A0}O1Y poiuav0a “y vingif “eA vyNgG?{ “(I ‘loso[Q, vIDsu0ja vyI0/hj}01(7 *IOSO[N) (Z[NYOS) souiw “IVA “Q “AV ‘pjv)NI1dv1q “IBA “BUILT (wuoy) vzp7nNI1dD1q sisdopnrianAy “‘Z[NYIS sour ‘J vyvynaidp “1eA vYyZUvIDIA] “(T ‘DIDPUNOL “IVA OSNOL DIDPUN}OL *(T ‘Daf -1]]9WD)] “ABA IOSO[H V4afipyjawn) “(7 "874 -UadDd "J 1OSA]) S]JUadDI “IRA “f "J “1) -jansuad{ “1WA “]Jaq Aljjenduasf -q ‘DINq -1f ‘y vynqif ‘eA “ayy Dongil -q ‘DID]a “IBA JASON) VJD}a vYI0/AjII(7 ‘J vyvjn21dv soroads SOIETTIBE YJOONTS a2us004q Aqreq 9us904 21e7 RIOT} wo1e Ip jo asy O2 NI SH LD SOD oD Co o G Vi € Vv € 3 S S G “I uot1 -enyeAd SATIe -luenb “gsnof 27777N “gS “RAOUISSIUY 22M0UNIs Siauouzdars ‘unity (‘qIoy]) supsajza snpnoiwapyy ‘S "YW wnsoj]nIidjuaa “J “gSNOf a7iqvdium "7 "SO CY Mayuly Wni}D4aI14 J ‘UNIND SN4OdoLIDUW “IRA 140]]00Uu * 9 ‘IY SN7DIUI) SNISi poulIso|D ‘unIyD Dipaw -4ajul “IBA Siding sixrfidouvyda,s *(surI0} jo dnoi3) -zyy (-ayy) V2VIINS D«ISOjapy ‘qsny (‘qleox) vidjnora viopUuIs J “ADIX) UWNIDULOLA WNIPDLIII J “asno ft SISua]DAN "A a Ne) SE Ps se) “TD ev puinuad “IRA snjpsofiad “yye “9 ‘afvd “eA “UNI Idahpd “9 ‘unin, snsodou -IDUW "IBA 14a]]a0W sSNnIsipoU1Is0] ‘UNI, DIPawsaqUr “IBA Siding? SF ‘asnor vzipa siridouvydays *(suJOJ Jo dnoi8) *zyy (ay) V7vI7NS DaIsOjay satoeds saxotduiod wioietp olsts19RIeEYD 34 on ‘aims Aoias | -woieip Arig gated 21TWI01 “aims 11q]] ~PIp o11yM ase oon ASotoyit1 Bale AOINS ‘Z9L [19M WOY sotduies Jo uoNIeUTUIeXS OTdodsOIOTWI Jo sI[NSeY “OL TIGWL 87 85 Slavgorod suite — Cr” °P 85.0—95.2 m Gray argillite with a slight greenish tinge, somewhat gaizelike, with siltstone and sand pockets on lamination planes; also with fine glauconite grains, plant residue, small calcareous tubules, and in some parts numerous worm trails. The rock splits into parallel plates with an irregular plane of fracture. In the 90.6 —91.2 m interval an interlayer of glauconitic rock with quartz gravel is encountered. 95.2—111.5 m Greenish gray, glauconitic-quartzy sands and sandstones are underlain by argillaceous rocks with pea iron ore. A total of 5 samples from this well were examined. One sample from the Slavgorod suite (no. 8, 94.2 m) and 2 samples from the Talitsa suite (no. 4, 48.4 m; no. 5, 57.6 m) showed no signs of algae. On the other hand, numerous algal remains were encountered in the samples from the Irbit and Serov suites (Table 16). Characteristic of the Serov suite is the abundance of frustules of Melosira sulcata (Ehr.) Ktz. (group of forms), Stephanopyxis turrus.var. intermedia Grun., Lriceratium, kinkieri A. Ss T. mirabile Jousé, and T.ventriculosum A.S. Frustules of the order Mediales appear in considerable amounts in this suite. A similar complex from the eastern slope of the Urals was described as Early Eocene. The silicoflagellate flora consists of 11 species, varieties and forms. Most abundant are skeletons of Dictyocha lamellifera Gleser var. lamellifera, var. constricta Gleser and var. hastata Gleser. The skeletons of D. elongata Gleser and D. fibula var. fibula f. eocaenica Krotov appear in smaller amounts. Finally, skeletons of Naviculopsis robusta Defl. are rare, and N. biapiculata var. minor (Schulz) Gleser, Dictyocha navicula Ehr. and three forms of D. triacantha Ehr. very rare. The diatom complex of the Irbit suite is characterized by the abundance of varieties of Melosira sulcata (Ehr.) Ktz., as well as Stephano- pyxis turris var. intermedia Grun., S. edita Jousé, Tricera-= tium exornatum Grev., and different species of Coscinodiscus. On the basis of these features, this flora can be placed in the Late Eocene. Dominant among the silicoflagellates are Dictyocha frenguellii var.carentis Gleserf.carentis, D.triacantha var. apiculata f. minor Schulz., D. rotundata Jousé var. rotundata, Navicu- lopsis biapiculata (Lemm.) Freng. var. biapiculata et var. minor (Schulz) Gleser; other species appear insmalleramounts. Table 16 shows that the Late Eocene silicoflagellate complex differs sharply from the more ancient complex of the Early Eocene. Well (rl, Gamararski11 "secror 0.0—15,0 m. . Ne.core: 88 Irbit suite — Pg?-9 15.0—15.8 m White diatomite, yellow-tinged, slightly micaceous, dense and heavy, with fine siltstone. At top of the stratum sparse quartzy gravel, rolled or partly so, is encountered. Contains large amounts of plant residue. Serov suite — Pg} 15.8 —64.1 m Light gray diatomite, lighter-colored below, slightly micaceous with small, very rare spots of ferruginization, and denser above. Thin lenticles and sparse interlayers of silty-sandy material are encountered, containing mica and plant residue whose concentration increases downward. Sparse quartzy gravel occurs throughout the rock. 64.1—73.1 m Light gray, micaceous, dense gaize, heavier than the above diatomites, solid and resounding on impact, breaks down into sharp-edged irregular fragments. Contains -numerous lenticles and pockets of a micaceous sandy material, which decreases appreciably downward. Areas of ferruginization around pyrite nodules. At the end of the stratum, there are oolitic inclusions of dark gray argillite, fine and sparse accumulations of glauconite and a large amount of fine, carbonized plant remains. Talitsa suite — Pg, 73.1—98.0 m Core extensively destroyed. Dark gray, micaceous argillite with numerous lenticular interlayers of siltstone and fine-grained, micaceous-quartzy glauconitic sand. Fine, carbonized plant residue is encountered. Fragments of sideritized argillite are found at depths of 92.1, 92.8 and and 95.1 m. Poor lamination. 98.0—114.5 m Core markedly destroyed in some places. Silty, light gray, micaceous argillite, in places somewhat gaizelike, dense; on planes of lamination there are fine siltstone and sparse, carbonized plant residue. The rock breaks into parallel plates with an irregular plane of fracture. 86 Slavgorod suite — Cr"? 114.5—119.0 m_ Dark gray and gray argillite, in places gaizelike, inter- bedded with greenish gray glauconitic sandstone resemb- ling Santonian sandstone. The rock is fairly solid and monolithic; a 30-cm-thick interlayer of gray sandstone with a slight greenish tinge lies at the bottom of the interval. 89 119.0—121.3 m Gray argillaceous siltstone, in places slightly gaizelike (possibly a diatomaceous siltstone), with laminae and thin lenticles of white clay; there are sparse masses of sandy material with mica and glauconite, and sparse carbonized plant residue. The rock breaks at angles up to: 20°. 121.3—128.7 m_ Dark gray siltstones with a considerable amount of argillaceous, silicified material. The siltstones pass into black argillaceous gaizes with a large amount of relatively regular lenticles of glauconite. In some places the glauconite spreads all over the rock. Lamination of the rocks is obscure. The rock breaks into parallel plates at an angle of 25— 30°. This zone is underlain by conglomerates composed of pebbles of eruptive rocks cemented by a brownish gray argillaceous mass and interbedded with gray and brownish gray coarse or mixed sandstone with glauconite. Four core samples of well 771 were examined microscopically (Table 17). Algal remains were found in the samples from the Slavgorod suite (no. 8, 120.6 m), the Serov suite (no. 2, 31.2 m) and the Irbit suite (no. 1, 15.5 m). No algae were detected in material from the Talitsa suite (no. 4, 77.0 m). Numerous diatom frustules and silicoflagellate skeletons were encoun- tered in the gray, gaizelike argillites of the Slavgorod suite. The dominat- ing diatoms are Stephanopyxis schulzii Steinvar. schulzii et var.cretacea Jousé, Hemiaulus asymmetricus Jousé, H. polycystinorum var. brevicornis Jousé, Trinacria anis- simovae Jousé and other characteristic species of the Santonian- Campanian of the eastern slope of the Urals. The silicoflagellates, represented by very rare or rare specimens, belong to only 4 species of the families Vallacertaceae Defl. and Cornuaceae Gem. (Table 17). -The gray diatomite of the Serov suite contains species constituting the dominant complex of the Early Eocene of the eastern slope of the Urals (Stephanopyxis turris var.intermedia Grun., Triceratium kinkeri: A: S., *T. mirabile:Jousé,(T..ventriculosum A, S.,, and Grunowiella gemmata (Grun.) V.H.). The abundance of Coscinodiscus lineatus Ehr., Trochosira spinosa Kitt. and Hemiaulus elegans (Heib.) Grun. does not contradict the conclusion that the flora belongs to the Early Eocene. The diatom complex closely resembles that of the Serov suite in well 564. There are 8 species, varieties and forms of silicoflagellates. Most abundant are the skeletons of Dictyocha lamellifera Gleser var. lamellifera et var. constricta Gleser; those of var. hastata Gleser and D. elongata Gleser appear in smaller quantities. D. fibula var. fibula f.eocaenica Krotov and Naviculopsis robusta Defl. are encountered rarely. Characteristic of the complex of the Irbit suite is the abundance of varieties of Melosira sulcata (Ehr.) Ktz., the presence of large numbers of Stephanopyxis edita Jousé, and the great diversity and quantitative abundance of Coscinodiscus species (Table 17). 90 (87) € "1aSa]) DIDISDY “IBA *] “CT y ‘asnof a71qvdim =“ f 7 *“19SO]) DJII47SUOI “IBA "7 “T G ‘SC "YW Mayurly WnI4D410914 J ‘Dial fé ‘unIy) SNIDINSUY sNIs1po0jI1;80pNas q c -1]]9UD] “ABA ISA] DsafiqJawy] * € ‘Iywey (‘AoIy) sisuauosow "yye 9 *A0}OLY G ‘IYY SnNzpau2y snasipoursso) Z pojuavo0a *y vjngif{ “AeA vjngif *q G ‘qyTypsouids vsisoyI04 J € “1OSO]H) VIDSuUO]a “(7 ‘und DIpaw A *19S9]‘) 3u900g 9 -Jajul “IRA Siding sizhdounyda,s Bq 21TWI01e1p I (zjnNYoS) vunIysjasunyosn vYyI0h}21q Aqreq G ‘asnof viadsp vsisopod ‘91TMs AOIES kein Z C “qsuy (‘qloy]) v7dynora vidovUis ) ‘unIy) snuDIs C -ou ‘IeA snydsowfjzod snjnviwayy G ‘ADIN) WNJDULOLA WNIZDLIII4 T ‘Jaso]y) (zpNYyoS) «ow Yy ‘1D ‘V vuinuad *iea snzosofaad *9 C -1u “IVA vyv]NIIdD1q sisdopNIiav Ay G ‘und snuodosovu “IRA 249]]20W *2 ‘DYJUDIDIA] “J ‘UNID) S140] Z DYIUDIDIA] “IRA “AUD DYJUVIVDIA] “(7 y -od ‘IRA suadsaizap snosipou19so) ‘S27 G ‘asnof vpyipa “ss G -UadDI "J JOSAH) S1ZUaLDI “IRA “{ “GT Z ‘unig 1yss01q sixidounydajs 11] e ‘UNIN) SNyDIpD4L snosipojvh 1 ~janSuaif “IRA “TJaq MpjanFuaa{ «cp | 249908 *(SUIIO} Jo g-god =| e1TWIOIeIp ‘p]D]a “IRA JOS@[) VIIa vYI0AIII(T aie] 9 dnox3) ‘21M (AY) 970I)NS D4ISO;ap ‘alms 11qJ] ay M J uot -enpeao uon -enyead satoads RIOT} satoads ‘ou ar WIO1eT cage age A8ojouit wi ‘yido etd -T1Uenb » -T1uUenb pure 91Ins yen baa ; Jo asy : -wes SOIC [2B ELJOOTTIS Saxed WO WOIeIp ITIstTI9IOeIeYD Pale AOIZS ‘TLL T[a” Woy satduies jo uoNeUIWIeXe SIdoOosoIDIWI Jo syNseyY “LT ATGVL 91 (88) Nm IAN -enyeAo OATIEI -Tluenb ‘Z[NYIS vppINfr47 “OD ‘JO vsafiajnov vnusog ‘euuep, Zajdwis vynwoshT “RUURT] 212U0]L0Y 0}4290]]0 4 ‘Taq visngos sisdojnaian yy ‘IY VyNolepu *q satoads Sd1LT[IBeYOOTIS uel -urduiesd -uPtuolUes aua90g Ayieg e1OTJ wo1eIp jo any wa MIN LD iene 2) ONWMMOMoANNs uotl -en[eAd aaTe1 -tluenb WALI Alc! WO snnbyup “yo snipv7y ‘asnof varvjaL9 vjpIxhg ‘undy vI1Uu ‘IRA D]]aJUOPO wnIIaY;01N0F ‘asnor vyiuifapur *f ‘aSNOf avAowissiuD DIMIDUIM J ‘osnor slu -lonlaadg “TWA wnsourshrhijod ‘asnof snjpynuiyoa “yy ‘asnof snoijawmufiso snjnviway ‘asnof 2z7NYyIS WN17V49I14 J ‘Z[NYIS snuossip sngsipouisso) *(A010I1H JOYe) Z[NYIS vjoULO *s) ‘OSNOL VaIDJa4I “ABA JO 2227NYIS “IBA ‘ULOJS 2IZpNYIS sixhdouvyda,g ‘HA (Cuniy) vjpwwas vpja1noundy) "BAOUISSIUY 2Mounse siauod. dang ‘unIy) 22Sss1am = DWUDAS0;0UNT ‘IyWOy (ued) vIIssns ‘qd ‘undly viqnp vip xhidopnasg ‘undy) (‘qIoy{) supsaja “yy ‘unIy SINSIQuyd snjnviwajy ‘Sg "YW wnsopnaiquar “J satoads saxad woo wOoIeIp OTIsTIDNIOeIeYD a1 [Ise aytpezies posoBarrs |ATays1s ‘eID 8 nN an 3d a1TWI01eIp ‘alms AOINS Arig Z ase is k3 ' Kissin oTouaty w ‘yidaq| etd -wes co fen) (panuuos) LI a1aVL ro 89 On the basis of these features, the above diatom complex can be related to the Late Eocene flora occupying a large part of the eastern slope of the Urals and the West Siberian plain. Only 5 silicoflagellate species, varieties and forms have been found together with the Late Eocene diatom complex. Most of the skeletons are of Dictyocha frenguellii-var..carentis Gleserf.carentis and Naviculopsis biapiculata var. minor (Schulz) Gleser; other species are represented by fewer specimens (Table 17). Like the diatoms, the silicoflagellates of this well form 3 sharply defined complexes: Santonian-Campanian, Early Eocene and Late Eocene. Verkhotur'e [Upper Tura River] area Well 13 Slavgorod suite — Cr," “°P Toadepthof24.5m Siderite and dense, compact glauconitic-quartzy sandstones. 24.5 — 26.5 m White diatomite is more silty and loose at the beginning of the stratum thanbelow. Therock is somewhat greasy to the touch and sticks to the tongue. Inclusions of fine scales of muscovite are observed. There are light gray, solid, light, "resounding" gaizes at the bottom of the stratum. Four samples of white diatomite were examined from this well. The material was collected at short intervals from 24.9—26.0 m (Table 18). All the samples revealed a qualitatively and quantitatively modest diatom flora. Only Stephanopyxis schulzii Stein. var. schulzii et var. cretacea Jousé could be characterized as abundant. The remaining species, even those characteristic for the flora, were represented by a limited number of specimens. Nevertheless, the presence of S. schulzii Stein., Melosira cretacea Jousé, Stephanopyxis antiquus Jousé, Coscinodiscus dissonus Schulz, Poretzkia mirabilis Jousé, Pyxilla cretacea Jousé and other characteristic elements of the Santonian-Campanian of the eastern slope of the Urals indicates that this complex is also Santonian- Campanian. Silicoflagellate skeletons, belonging to a total of 9 species, varieties and forms of 4 genera and 3 families, were found in all samples. The family Dictyochaceae is represented by Dictyocha triacantha Ehr. var. apiculata Lemm.f.apiculata andvar.inermis Lemm. f.inermis, appearing very rarely and in some samples only. Most of the silicoflagellates are of the families Vallacertaceae Defl. and Cornuaceae Gem. Vallacerta tumidula Gleser and Lyramula furcula Hanna are most widespread, being found throughout the diatomite layer in con- siderable amounts. Skeletons of Cornua trifurcata Schulz were found in all samples except no. 1, and are more abundant in the lower part of the stratum. 93 (90) _ ros < = NSO ABWOWMI ANN =F 10 <= uotl -enpeaa aATI1e1 -tluenb *‘Z[NYIS vpvIWNfi47 DNULOD ‘euueyy vynoin{ vpnwosh'T “LaSo]H VpNpiung *4 “VuURHL 12U07L0Y 07L99D]]10 4 ‘Dipjnridv "} “WUWaT 7D) -nvidp ‘IBA DvYy,UvIDIA? DYIOAIIIC ‘ZINYIS = pyDIANfi47 YNULOD “euuRey, vynoun{ vynwoshT "1OSO[) VINPIWN, Yj41990]]0 4 “sr -4aUu) “JY “WWOT siuwsau? “IRA “7 'G ‘Dippnaidp “} “WUIaT DID] ‘IVA DYIUDIDIA? DYIOAING ‘zynyS vzpvIINfI47 *D ‘LOSo]H avlvyzjaLod ynusog ‘euueyY raydwis *7 “euuRey, vjynoun{ vjnwosh'T ‘IOSo]) VpNpiwnz “4 ‘asnor rajdwis *4 “RUUBFL 22U0)]40Y D)]L90D)2]0 4 -noidv ‘Dyppnaidv *} “WWay 27D) -noidp "eA vyyUDInI4] = DYI0hI21q7 ‘euuR_, vynounf{ pjynwoshT ‘IOSo[ VjNpruny “4 “BUURP] 12707404 D)4990]]0 4 satoods SOILT TAB eTJOOTIS ‘asnof vaInj,a49 vIDITAg ‘asnof avaowissiuD DI49DUIs J ‘asnose SsnIijaumufsp snynviwapzt ‘Z[NYIS snuossip snasipourss07 ‘aSNOL VaIDJALI “IBA JO NZNYIS "TWA “Uld}S W2Z7NYIS * ‘asnor snnbizup sixidouvydais uet -uedure5 -ueI CD elit at -uolues ‘gsnop sipsoaf “yy ‘asnof snaiwjawwhsp snynviwapy ‘ASNOL SI71QD4IU DIYZIAL0g “Z[NYIS sNuossip snIsipourss07 ‘OSNOf DIID}ALI “IRA 1IZPNYIS “IRA “UTIYS 1Z7NYIS +9 ‘asnor snnbijzuv sixfidounydazg uvT -ueduiey -ueT In =e OU NID _ uy -uoques ‘asnor sipispaf “yy ueT ‘asnof snaiwjawwfsy snjnviwayy ‘Z[NYIS sNuossip snIsipoui9so ‘OSNOL VaIDJAI “IRA Jo 11Z7NYIS “IBA “UIOJSG Mz7NYIsS sixfiidounydals ‘ASNOL VIIDjJaI VsAISO]A -urduiey -uveI -uoques uet ‘asnor SNIMjawmMfisp snjndiwa py -uedwied ‘Z[NYIS snuossip snosipouisso7 ~ueT ‘OSNOL VaIDJA4I “ILA YO 11Z]NYIS -uoques “IBA ‘UIBJS Mz7NYIS sixidouvydarg uo -rn[eAo RIOT] satoads wu01k Ip jo asy SATE -Tluenb soxatduiod wioieIp dTsTIANIOvIeEYD BOIE 9,INIOYYIOA 91 UT ET [TAM Wo satdures Jo UOTIeUTUIeXD DIdOodsOIOTUI Jo siTNsoy z do-ys-ug49 ‘poloBArTsS do-1s-ust9 ‘poiosAe{s z Ze) ‘PpOIOSARS do-1s- ase pue ans dITWIO1eIp a1TyM j S a]TWI01eIp 1T4M y dITWI0e Ip oTyM ; G 211UWI01e 1p am1yM : | ‘ou ASojouary wi ‘yadeq]| ad -wIes “8 ATAVL 94 91 The complexes are qualitatively and quantitatively quite similar. Although no. 2 shows a somewhat different assortment of species, these are quantitatively insignificant and do not affect the general nature of the flora. Area of Makhnevo village Samples from wells 85, 90, 528, 547, 567, 1479, 1481, 1482 and 1503 were examined. Algal remains were detected in some wells only. Wet S00 Kokugekii sector, siowth of Makhnieyo Quaternary deposits 0.0—11.0 m Grayish brown loams. Talitsa suite — Pg, 11.0—25.0 m Gray, sometimes slightly greenish, silty slightly micaceous argillite, in some parts gaizelike, with laminae and lenticles of a sandy siltstone with glauconite and mica scales containing worm trails, sparse, fine calcareous tubules, fish scales and pyritized plant remains. The rock breaks down to parallel plates with an irregular plane of fracture. Lamination is horizontal and poorly defined. Slavgorod suite — Cr;" “"°P 25.0.—36.0 m, Light gray and gray, greenish-tinged, silty, very slightly micaceous argillite, in places with a considerable concen- tration of worm trails and interlayers of very slightly gaizelike siltstone containing numerous grains of glauconite and fine grains of quartz. Fine, pyritized tubules were _ encountered. The siltstone interlayers are up to 0.5 m thick and contain fish scales, carbonized plant detritus and pyritized remains of herbaceous plants. 36.0—39.5 m Gray, greenish-tinged, fine-grained, glauconitic-quartzy sandstone. A total of 8 samples from this well were examined. Four samples from the Slavgorod suite (no. 5, 25.2 m; no. 5a, 28.5 m; no. 5b, 31.3 m; no. 8, 37.8 m) and 3 samples from the Talitsa suite (no. 2, 16.5 m; no. 3, 20.3 m; no. 4a, 24.5 m) showed no algal remains. 95 Algal remains were found in the upper part of the Talitsa suite ata depth of 12.0 m (no. 1), which contains a poorly preserved diatom flora consisting of the following forms: Quantitative evaluation Melosivra sulcata var: siberica Grun,. . 7a as Stephagopyxis ferogeerer.) Ralfa. & 5 oe see aa S. T#Eris “vari inter wmetia Gruns~ 5s (ee fa A Hemiaults® poly cystminmor wm "Gruner shee: : Trinacria pileolme*bir.var. pileelus 7445. . ie Tt. Pp. Vals JOPCP Ree Barun... be te Sh Be BR tes, ws Hemiaulus polymorphus var. frigida Grun. RRR PB PR Ww “ll these forms are characteristic of the Early Paleocene of the eastern slope of the Urals. _ The silicoflagellate fauna consisted of 3 varieties and forms of Dictyo- eha triaecantha Ehr., of which var. inermis ‘tf. minor ‘Gleser and var. hastata Lemm. were especially numerous. Well 547; Vinokurovskii Sector; Makhnevo village Quaternary deposits 0.0—10.0 m Grayish brown loams. Serov suite — Pg} 10.0—20.0 m Light gray, firm gaize splits into sharp-edged, irregular fragments. Talitsa suite — Pg, 20.0—30.0 m Core extensively destroyed. Gray to light gray, vaguely fine-layered, gaizelike siltstone, breaking into foliated units, contains sparse, fine scales of mica. 30.0—50.8 m Gray, light argillite with a large amount of siltstone, fine plant detritus and mica. Lamination is fine, horizontal. The rock breaks down to parallel laminae. 50.8 — 55.0 m Light gray, slightly greenish-tinged, somewhat gaizelike diatomite with siltstone mica, fine plant residue, car- bonized plant remains and numerous worm trails. 55.0—56.0 m Light gray, very firm gaize with a small amount of silt- stone, fine plant detritus and carbonized remains of herbaceous plants; worm trails occur. The rock breaks into irregular, sharp-edged fragments. 96 92 56.0—60.0m__ Light gray, argillaceous diatomite with a small amount of siltstone, sparse worm trails; the underlying rock is more solid, silty, and gradually passes into sandstone with interlayers of looser silty diatomite. 60.0—67.2 m Light gray, fine-grained, moreor less argillaceous, firmly cemented sandstone with mica scales, glauconite grains, pyritized plant debris, isolated worm trails and fish scales. At 65.2 m there is an interlayer of glauconitic-quartzy sandstone with sparse quartzy gravel and fish scales. 67.2—74.5 m Light gray, sometimes slightly greenish, argillaceous siltstone with mica scales and a large amount of partly rolled quartz gravel with sparse plant detritus and worm trails in places. Slavgorod suite — Cr," “°P 74.5—79.0 m Light gray, somewhat greenish-tinged argillite with pyritized remains of herbaceous plants and rare fish scales; there are "prisypki'' of micaceous and silty material on the planes of fractures. Lamination is clearly horizontal. A total of 12 samples from this well were examined (Table 19). The material from the Slavgorod suite contained only partially dissolved fragments of Gladius sp., but no traces of silicoflagellates. Well preserved diatom frustules and silicoflagellate skeletons were found in 3 samples from the Talitsa suite (no. +17, 59.9 m; no. 10, 5038;m;) HO. 3, 33.0 m). The intermediate zones (36.83 m, no. 7; 38.4 m, no. 9; 53.8 m, no. 12; 57.4 m, no. 14, and 58.9 m, no. 16) contain very poorly preserved diatom frustules and no silicoflagellate skeletons. The above samples (nos. 3, 10, 17) showed an almost identical diatom flora with differences mostly of a quantitative nature. Stephanopyxis turris var. cylindrus Grun. et var. intermedia Grun., Coscino- discus lineatus Ehr., Triceratium heibergii Grun. and Hemiaulus polycystinorum Grun. are abundant everywhere. The density of the following forms decreased rather sharply upward in the section: Stephanopyxis lavrenkoi Jousé, S.ferox (Grev.) Ralfs, Hemiaulus ambiguus Grun., Trinacria pileolus var. jose- phina Grun., T. regina Heib. var. regina etvar.obtusa Witt. On the other hand, the density of Hemiaulus polymorphus var. frigida Grun. increased upward. In addition, valves of several species of the order Mediales — Sceptroneis wittii Jousé, Grunowiella palaeocenica Jousé — were very abundant in the upper layer at a depth of 33.0 m. This diatom flora can be placed in the Early Paleocene on the basis of the similarity to the corresponding diatom flora of the eastern slope of the Urals. Since the complexes in all 3 layers combine features of the upper (abundance of Triceratium heibergii Grun.) and lower complexes (abundance of Hemiaulus polycystinorum Grun.) it is not certain to which complex they belong. Another characteristic aspect of the complex are the abundant frustules of Coscinodiscus lineatus Ehr. 97 (93) NO N19 oD uoll -enpteAd ATE =-T1uenb Ped (zjnyos) vyojna1dpd “yye vuasosayy “IOSO[X) LOUIU “J SIW4aUI “IBA "7 “(7 “STU -4aul “Jy “WUT siwiaul “IRA 7 “°C "UWaT vIDISDY “IRA "7 “CT *Z[NYIS LouIwW *} vID]NIIdD “IBA "7 “CT ‘pyvyn21dv ‘J ‘WuloT vypjnaidp “aRA "7 (J “‘DYJUDIDIAZ "J DYJUDIVIAZ “LBA “IYO DYZUDIDIAZ “(7 ‘asnof vypoun{ “(7 “19S9[D (z[NYyOS) vuviysjasuvyoun DYyI0h}21q7 satoeds SOILT[IBETJOOT[IS PIO] woe Ip jo o8y ‘saTeNUaD Iapio dY2 JO SUIOILIP aUTIeW Jo sIuOU -Selj OUTy BPQeIUApTUN paivjos|| ‘arts esiTe LT ATIB1y ‘asnof DI1UaI0aD]Dd D}JaINOUNAY ‘UNIN) DIIpunzIN[ “IBA DIN}JAIUD) “Y ‘asnof v217d1))2 siauoydnyy ‘asnof 227710 siauouzdaag ‘aSNOf VII)VIN DIAYIOLaZ “VIT Ur VAOUISSIUY S2D2D9S v)pIxhdopnasg “IY VIJA7UOPO wNIIdY,01IUOH “‘VILM BSN7IQO "IRA “4 +7 ‘puis -al “ABA "QlOf{ DUIsAd DIWIVUIMT und) Dpiziaf “VeA snydsowfhjod * 7 ‘unin Wnsourshoijod +} ‘unInND SnNFiquo snpnviway “UNID) 11940ag1aY WNIVD4AII4 J ‘suo (‘und) pioydojoqufis “IeA Ssi4D]]a}8 "9 ‘IY SNppeUI) snosipourss0) ‘UNID) DIPaMsazUul “IRA qo ‘Und') Snapui7 ha “ted Si4in} “ ‘asnof 10yuaian) “5 ‘syjey (Aery) rosaf sixidounydazy9 | ‘aims esate L ST T1S1V uotl ~enTeAe satoeds aie oe aan AZojoy311 |w ‘yideq| ard -Tluenb BOP Pathe -wes ML NN C wr saxotdwiod WoleIp O1IsTIsIOVIeYD Pole OADUYYARW ‘LPG [[T@M Woy satdures jo uotleururexs dtdodsosIOIW Jo si[Nsoy “GT ATAV.L 98 G ‘TJ9d (zjnyoS) vivjnNIIidv ‘je vUaI0say 1 "STU Zz -4au) “J “WUOT Siwwau? “IRA “7° “WWaT vIDISDY “IBA “] “GC J Zz] NYS 4oulm "y vyvjnaidv "IRA "7 “G if ‘Dypjnaidp *y if ‘WWdT v7Dj]NIIdD "IeA DYJUDIDIAT “(7 ‘asnof vzvI4n{ vYyI0hj21q uoll -enyeaad : satoods dAT1eI -T]UenNb $91 PT [IB PYJOOTNTS (94) “sJUDUISEY B[BUISs Btqeyiueptun ‘ouy pue ‘Zlor (‘undy) vuoydoj0qg -wfs ‘IeA $140]]2]8 snasipourd -oj ‘ds vidavumy ‘ds snynviw SIUSUIBeIJ P2Ie]OST ‘TTeUIS ‘QVM Suardisur visovUuId y QUd909T “ds sizidounydajg9 enptatput -vg Aieg ‘surojeIp padrasaid ApI00g ‘IYY VIJa2UOpO wmni9aYy,01U0H "VVIM DSNZQO “TWA “4 I ‘DUIsaL “IRA ‘QIOH{ DUIsaL 7 ‘und puiydasol ‘1eA snjoajid vi49pUIdT ‘unin Dpisif ‘Ira snydiowhjod * yy ‘unig, wnsoulshoijod "yy ‘UNI, snnsiqup snjnpiwa fT UNI) 2288192 “ff “UNID 225499104 WNI4D49IIA T ‘B19 (‘unID) pioydojoqufs “IeA Siapjjas “9 “IQ SNjpauiy snIsipouisso7 ‘ds Ss ‘UNI DIPawMsajqUr “IRA “7 9) ‘undIy) smupur7Ad “IRA sitang * 5 ‘aSNOf 10yUuatavj] “9 ‘sypey (Aor) rosaf sizidounydazg 2Ug902T -eq Apieq 2Ud902| -eqg Apieg SUTPUIOI WIOIPIP eTqGeTJMUepIuy uoll -en{rAad RIOT] satoods ATIF wWIO1eIp -Tluenb jo o8y saxo[d Wood WOIeIp ITIsTIAIOevIeYD ‘aiins esiite L 1834 ‘a1Ins eslITe L ™3q ‘ois esitte L 21TWI01eIG ; by} aIwoieIq i ZI ‘oumsesiqeL} = aaty[tBry OF a1tTTIB1y 6 ‘ou wi ‘yadoq} etd -uIeS ase Bie ofr AB0joyiT (penutqu09) 6 ATAVL 99 (95) uor} -en[eAa dATP -Tluenb *s1u -4aul "Jy “WWOT S2uwdaur “eA 7 *° “WUT DzDISDY “TBA “2 “(CT *Z[ NYS Loulw *y vjvjNII1dv “eA *} “7 *pypjnoidp ‘J “Wwley vyvjnoidp “IRA ‘7 ‘Q ‘DYIUDIDIA} *Y DYJUDIVDIA] “IVA “AY VYPUDIDIAD “(7 ‘asnop vypounf{ “(7 "19ST (z[NYoS) DuvIysjasuvyodD DYI0A}I1(] sotoads SIP [TAB eTJOOTTIS N te) mcoiwmwoninm wD Tu LO LN 9uU2909] -eg Apsieq uon -eny[eAd RIOT} woe Ip jo o8y aATIeI -1Tluenb ‘poXdonsap Aired ‘ds smipvj7y Jo saateA a[8uts ‘asnof voIUav0anjpd v2j]a1NoUnNIH "VIM. DSN7QO “IRA “4 OT ‘pursat “IBA “QlayT DUuIsas * 7 “uniy puiydasol ‘Iva snjoajid vi4ovur. J ‘ung vpisiuf ‘wea snydsowhjod «77 ‘unig wnsourshohjod * yy ‘unInD snnziquo snpnviway ‘UNIN) 181ag1ay wnI7vL9924 ‘IOSO]) DIDUOQUN D1IY21240q ‘Blof (‘uniy) pioydojoqufis “IRA $240]]278 *O ‘IY SNypeuI? snasipoui9s0) ‘ds sixfidouvydai9 ‘UNI DIpamsazur “IRA "7 *S! ‘und snupurjfd ‘eA siding *s) ‘asnof 10yualav) *S' ‘sypey (Aery) rosaf sixidounydaiy sapnisnay woIetp paazosstp Aqyetued ‘ayqeiymuepruy satoads saxeaTdwiod WoIeIp ITIsTIDIORIeYD z do-3s-ud!9 ‘itns po1o8arts '3q ‘aims esiipte L Sq ‘oimns este L ase pue a1mns aI TB1e pesun 8Z -ystuse8 ‘Ae IYST] cz aITITBIV i LI AITTIBIV 9} ‘ou wi ‘yidaq}] otd -wes A8oyoyI 1 (ponutuos) 6T FIV. 100 A fairly uniform silicoflagellate flora accompanies the Early Paleocene diatoms. Only 4 species were found — Dictyocha triacantha Ehr., D. archangelskiana (Schulz) Gleser, D. furcata Jousé, Mesocena aff. apiculata (Schulz) Defl. The first species was represented by 6 varieties and forms. The samples showed an algal flora of roughly uniform composition, although the numbers of skeletons increased upward in the section. This was most pronounced in Dictyocha triacantha var. hastata Lemm. In addition, the number of skeletons of D.triacantha var.inermis Lemm. f.inermis increased from very rare to frequent, and there was a Slight increase in the density of D. triacantha var. apiculata f. minor Schulz and D. triacantha Ehr. var.triacantha Ftriacantha: Well 1482, north of Makhnevo in the Tura—Tagil interfluve Quaternary deposits 0.0—14.7 m Yellowish gray sands interbedded with dark brown loams and fine-grained, dark, grayish green sandstone. Some horizons contain quartz gravel and well-rolled pebbles of gray, heavy gaizes. Talitsa suite — Pg, 14.7—52.9 m Gray and light gray, micaceous in places, silty, slightly gaizelike argillites with glauconite grains, individual fish scales and small fragments of calcareous shells. 52.9—53.6 m Quartzy-glauconitic, strongly argillaceous, firmly cemented sandstone with lenticles of quartzy siltstone and glauconite; quartz gravel and inclusions of eroded carbonate rocks, and sparse fish scales are encountered. Slavgorod suite — Cr," *"°P 53.6 —61.1 m Light gray with distinct greenish tinge, gaizelike, greasy argillite breaking down into parallel plates; pyritized remains of herbaceous plants and small, dark concretions occur. Argillites contain more siltstone lenticles with glauconite grains and worm trails at bottom of stratum. 61.1—6451 mi Fine-grained, quartzy-glauconitic sandstone. 64.1—66.7 m Light gray with slightly greenish tinge, micaceous, argillaceous siltstone with vague, finely undulated lamina- tion and containing fish scales, sparse plant detritus, isolated fine fragments of calcareous shells, and small lenticles of a quartzy-glauconitic material. 101 (97) N ine) N Ns on NN uot] -en[eAd aATIe1 -T1UeNb TP (zjnyos) vyvjn21dv “yye vuav0sayy ‘TOSO[N) LOUIW “} SIWwaUI “IRA “7 °C “S1U -4aUul "J ‘WW Siwdaur “IeA "7 “G7 ‘WUATT ~DIDISDY “IVA “7 “GV “Z[NYOS Louw "| DID]NIIdv “IeA "7° ‘pypjnaidv ‘} ‘wuley pjpjpnzidp ‘1eA *7 “ “DYJUDIDILD “Y DYJUDIDIA] “IVA “IY VYJUDIVDILG “(J “1ase]y (zjnyoS) vuviysjasunyoun vyr0hj21q ‘TJ (zjnyos) vzDjpn21dv “ye vua20say “19s -O[) 4oulm "Jy Srwsaur “IRA “7 ‘C7 “s7ul -daul "J “WIUWOT Siwsau? “IRA "7 °C “WUT DIDISDY “IVA “7 “CZ *Z[NYIG LouIw “jy vJDpNIIdD "IBA *} “CT ‘vypjnnidn *y ‘WWay 07D)NIIdD “IVA DYJUDIDIA]Z “CT “19S9]H (zjnyos) vuniysjaszunyouv vyI0hj01(7 “ZINYIS 4oulw *} vzv] -nndp ‘IeA vyjuvoni4, DvYyI0hq21q sotoads SOIL TT ABETJOOTIS UNIX) Diafiui4Dd DvIaY}0L9]g “D1 9]UOpoO ‘WA ‘“IYY YJjazuopo wmn29ayj,01U0y ‘uni puiydasol “18d snjoajid vidgvUIdy ‘unin wnsouljshohjod snjnviwayy "S$ "Y wnsopnaiajuaa “J STEM Wssiem, oT ‘UNID) 1294ag1aY WN17ZD4a9I4 T ‘IYA SNjveui] snasipouisso) ‘UNIN) DIpaudajul “IBA Siang “9 34 aussie ‘SyTeuy (Aoiy) xodaf sixAdounydaz ys | ‘tains esiye 1 Aas ; 20) OD 9 OD 1 CO ise) ws 9U9902] -eq Aqieq oO oD ‘qloH YIVAvITa DidIDUIAT ‘unInn wnsourshoijod snjnviway UNI) DIpawdajul “IRA siding “9 ‘UNI SNupUrjfd “TRA si4ung “9 ‘sypey (Aad) vosaf sixidouvydazs 2usd002| *eIOLJ 134 ase -eq Aqieg paasasaid Aji00d ‘paystiaaoduit uy | ‘aims esate L SNITeZIeO P POT oD OD SD <4 OD aud909| *Ja19eIeEYO DUdI0aT eg Bq 6 -vg Apied JO BIOT} poysts1sAod wit-satoeds | ‘a1tns esiTe |, SIT TI81y }; uoll -enyead P1OTJ satoads ‘ou SATIFI : ase w01e Ip ASojouity |w ‘yideq] atd -Tluenb pue a1ins Jo asy -wes Saxa[dulod WOIeIp ITISTIDIDeIeYD BoIe OADUYYALIN ‘ZEPL [12M wor satduies jo stsXjeue o1doososo1w jo synsay ‘Oz AIGVL 102 =< N N N st st woN om sto wmoN uoTl -enyeAa aATIeI -Tluenb Td (zjnyos) vyvjnIIdpv ‘je vUaI0sayy “IOSO[X) LOUIU “J Slw4auI “IBA “2 °C “S17 ‘J ‘UIWAT s?wiaui “IRA “7 “(7 ‘MWeT vzDISDY “IVA “7 “CT *Z[NYIS Louw *} v7D]NIIdD “IBA “7 *G *pyp)n21dv ‘J ‘WwWeyT vvjnNIIdp ‘IeA “7 "GC “DYJUDIDIAZ “¥ DYJUDIDIAZ “IEA “IY DYJUDIDIAZ “(CT "1ase[D (z[nyoS) vuniysjasunyoun vyI0hj21q ‘euueT, vynoun{ vynwoshT Wd (z[nyoS) vywjnI21dv “jye Duaoosay "IOSO[) LOUIW “J SIwd4auI “IRA “2 “(7 *S1U -4aul "J ‘WUaT siwaur “eA "2 “(7 ‘WUlaT DIDISDY “IBA “7 “CT “Z[NYOS ourw "yj vjvjnNI1dv “IEA ‘2 “J *pyo]nI1dv ‘J ‘WwWeyT vpjn21dp ‘IeA 7 'G ‘DYJUDIDIAZ “J DYJUDIDIAZ “IRA “IU DYJUDIDIAZ “CT *Iase[D (zjnyOS) vuviysjasunyouv vYyI0hj21q7 -1au2 sotoads SaIeT [ABE TJOT IS aua902] -eq Aqieq 9U2902] -eg Apieg PIOTJ wo1eIp jo asy SHO OLON OD oO OD O19 19 1 ois MmMowmmwn wo uot} -en[eAd eATle1 -Tluenb “VIM DSNAGO “IBA DUIZAL * 7 ‘unin, vurydasol ‘ieA ‘d “7 *8N]02] -1d ‘1eA ‘IY Snpoajid viw9vUI4 ‘unin, wnsourjshohjod snjnviwapy ‘IYY $nzpauI? snosipoui9so) ‘UNID) DIpawmsaqUl “IRA 7 “GS ‘unIxX) Snupuijfd2 “eA Siding “G ‘syey (‘Aorn) rouaf sazidouvydajg ‘unInD DiafiuidDd DIaYI0La}q "VIM DSNIQO “IBA DUIsaL * 7 ‘unin vurydasol -1eA ‘d “7 *$n]0a] -1d ‘IeA “IYW snjoaid visovurs J uni) = wnsournshohijod snjnviway “JIM 2SSIam "7 "Ss "YW wnsojndidquaa * 7 ‘UNI 129499104 WNI4D4L9914 ‘BIof (undy) pioydojoqufis “1eA $140]]278 “Jye *D ‘asnof snyvipparas *9 ‘IY $NzVaUI]? snosipoui9s07 ‘UNID) DIpawsajur “IRA “7° ‘UNIX) SNUpUuI,Aa “IRA s1lln} “9 ‘sypey (‘AerD) zosaf sixidounydas satoads saxe{duiod WioleIp OTIsTISIORIeYD 134 ‘O1Ims PeslITe 134 ‘21Ins es1TTe L ase pur 21mns SIT T1B1e atts 21h a{[IB1e Aaqts QV) ‘ou wi ‘yidoq|} etd -uIeS AS8ojoultT (penunuos) 0% ATAVL 103 2ud909] -eq Aqieg 2ua009| -eq Aqieg Zz ‘UWA DIDJsDY “IBA DYZUDIDIA? “CT *IOSO]*) aUsa902] J (z[NYoS) vuniysjasunyoun DYyI0h}21q neg Apea ‘Wd (z[nYyoS) DyvpN21dv “jye Duavosayy “19s -8[) sourm "y Siwiaur “IeA 2 “GQ “STU -daul "J “WUWAT] Srwiaur “IRA "7 “GJ ‘WUWaT DIDISDY “IBA “2 “ “7Z[NYIS doulm ‘J vyoynaidp “1eA “7 ‘Q ‘Dyojnaidpv *y ‘UWA D7D)NIIdD “IRA DYJUDIVDIAZ “J “1aseTD (z[nYOS) Duviysjpasunyouv vYyI0hj21q ‘euuReE, vynoun{ vjnwoshT “eUUe TE, 22U0710Y D7499D]]0 4 2ua902] -eg Apieq Peloed eel els Beh. orktel > b~ wud uonl uon -enpeAd -en[eAad soatoads RIOT} aaTIeI aATIeI wo1e Ip -tluenb -tluenb jo a8y SAI T[ABeTJOOT[IS (99) Saxo[d Woo WOIeIp dTsTIAIORIeEYD *89]D4JUIDQ IBPIO ay Jo dsateatig > SWIOIVIP SUTIEL JO SaTNasny apqey ‘ams -Tqueptun ‘paarosstp Aq~enred ‘pareqos] PpOIOSAr{S SI TIBIV eal ‘UNID Dipamsajur “IRA siuunq sizidouvydagpue'ds snip | do-1s-uS10 -D] JO spua Jour ay Jo ‘aitns s]UdWIB ey poaatosstp ATT et1Ied ‘pairypos] PpOJOBARTS ATTTIBIV ai paarasaid Atiood 134 ‘eIO[J WIP sUad0aTeg poysTIeAoduy] | ‘a1mMs vsiTe L ATTTIBIV a *p]]a1UOpo ‘TWA ‘IY Vppazuopo wni9ayj0IU0y ‘unig vurydasol ‘rea ‘d "I *$n]} 0a} -1d ‘IeA ‘IYA snzoajid vr9IvUI4 J ‘uniny vpisiaf ‘rea snydisowfhjod * yy uni) «wnsournshoijod snjnviwapy ‘FIM 11SSiam “TL ‘S "YW wnsojnridjuaa “7 “UNIN) 194ag1ayY WN17VD499I4 J, ‘asnof snyvippixas *Q ‘IY $snNzpaui? snasipouissog ‘UNI) DIPausaqur “IRA ‘7 “SG ‘unIy) smupuijyia “1eA siang “9 ‘asnof 10yUuadavy “¢ "syTeyY (Aen) vosaf sixfidouvydas 184 ‘a1mns esiite L aitp {tse Aats satoads ‘ou wit A8ojoyutT =| wi ‘yideq} ard pue aims joy q I -wes (panunuos) 0% JISVL 104 66.7—68.2 m Dark gray with greenish tinge, very solid, monolithic, heavy, micaceous argillite containing a large amount of glauconite, small lenticles of light-colored siltstone with glauconite, and an interlayer of fine-grained, quartzy- glauconitic sandstone at a depth of 67.1—68.2 m. 68.2 —72.3 m Dark, greenish gray, quartzy-glauconitic sandstone. 72.3—90.1 m Weakly cemented, light gray, argillaceous, micaceous siltstone with quartz gravel and single fragments of mollusk shells underlain by a weathered crust. From this well 13 core samples were examined (Table 20). Twosamples from the Slavgorod suite (no. 14, 55.0 m; no. 14e, 59.5 m) contain diatom frustules in a very poor condition; no algal traces were found in the re- maining samples. On the other hand, there were numerous and well- preserved algal remains in the rocks of the Talitsa suite at a depth of 34.8 m (no. 10c), 37.4 m (no. 11b), 40.2 m (no. 1le) and 43.3 m (no. 11g). Table 20 shows that the characteristic complexes here consist of Early Paleocene species typical for the eastern slope of the Urals. All the samples (except 10a) contain numerous specimens of Trinacria pileolus Ehr. var. pileolus orvar. josephina Grun., Hemiaulus polycysti- norum Grun., but are poor or lacking in Hemiaulus polymorphus var. frigida Grun. These features are reminiscent of the lower complex of the Early Paleocene. However, the lowermost sample (no. 1lg, 43.3 m) is richin Stephanopyxis ferox (Grev.) Ralfs and Triceratium heibergii Grun. and also contains a relatively large amount of Ste - phanopyxis lavrenkoi Jousé and Triceratium weissii Grun. Such a proliferation of these species is characteristic of the upper complex 100 of the Early Paleocene. On these grounds, the encountered diatom complex can be placed in the Early Paleocene. Among the dominant forms is Coscinodiscus lineatus Ehr. Also noteworthy is the comparative abundance of Triceratium ventriculosum A.S., which according to Krotov, is also characteristic of the Early Eocene. Table 20 shows that silicoflagellates are most abundant and diverse in samples containing a rich diatom flora. Varieties and forms of Dictyocha triacantha Ehr. predominate qualitatively and quantitatively, especially D.triacantha var.inermis f. minor Gleser and D.triacantha var. hastata Lemm. The density of the latter variety increases upward in the section. D. triacantha var. apiculata f. minor Schulz, D.triacantha var.inermis Lemm.f.inermis and Mesocena aff. apiculata (Schulz) Defl. are more abundant below. The numbers of Dictyocha archangelskiana (Schulz) Gleser increase upward from very rare to frequent, and then decline to very rare. All samples contain small amounts of D. triacantha var. apiculata Lemm. f. apiculata, and isolated skeletons of Lyramula furcula Hanna and Vallacerta hortonii Hanna occur in the two lower samples. 105 (101) —=N N<_ —<— uotd -en[PAa dATIEI -Tquenb ‘Tyo (zjnyos) vypjn21dv “jyR biaent *IOSO[) LOUIW “J SIW4aUI “IRA “7 “(7 "STU -daul "J “WIUWOT Siwiaul “IRA “7 “(7 ‘UWA DIDISDY “IBA “7 “CT ‘z[NYyOS soul “} vz] ‘IEA DYyQUDIDIA] DYI0h}I1(CT— "eUUeE] 1107104 D7429D]]D 4 -noidv “IOSO[D) LOUIWM *y SIW4aUI “IRA “7 “CT *s1 Ul -4aUul "J “WULATT Siwiau? “IRA “7 “(7 ‘WUle] vIDISDY “IRA “7 “(7 “Z[NYOS sourw “IRA DYIUDIDIA? § “CT ‘asnor vypoun{ “7 “1asa[y) (2zjnYyoS) vuviysjasuvyouv vYyI0h}21(7 "BUURP] 11U0j10Y DZ4990]]0 4 ‘J DyvjN21dv satoads Sale [as eYOortIs (19UZARPq *S*A JO UONIDaT[OO 9y1 Woy) vary OADUYYPW ‘10199S TIysuUOyNA ‘EOL [aM Woy satdures yo uoTIeUTWeX DIdodsOIOTU Jo sIpNsoy PIOLJ wo1eIp jo ony or 1 60 1 OD SS wd uw sv € 5 (5 9 5 G wD uoll -en[eAd aAnel -tluenb "VYIM DSN7QO “IBA DUIZAL * *sn] 09] -1d ‘IeA ‘IY Snpoajid visIvUId T ‘unin =wnsoulshsijod snjnviwayy ‘UNI 118S1aN wWNIZDLaI14 J, ‘UNID) Dipamsajur “IeA Siding “9 ‘aSNOL 10yUadaD] “9 ‘sypey ((Aary) rosaf sizidouvydas ‘undy DL1S0]39 Jy DyD14a81q "“JWA DzVIINS “VIM DSN7IQO “IRA DUISaL * J *snjoa} -1d ‘IRA “IY snzoajid visIvUrd J ‘unInn wnsounshrijod snjnviway ‘UNID) 118S1aN WNI}D49I14 ‘UNIQD DIpPamsaqUi “IRA Siding “9 ‘asnof 10yUaLany *§ ‘syTeyY (‘Aerny) rosaf sixfidouvydays “undy) DIDI4IS1Q “IRA DIVIINS DISO]ay satoods saxaTdulod WOIeIp ITISTIDIDeIeEYD 84 a1tpSre a1IMs eSIITe L Kein 13g Aeyo sno ‘aiins esile L | -a0ewioieiq ase k San aire Zopoyay wi ‘yidaq| ad -wes ‘T@ ATAVL 106 102 Well 1503, Yukonskii sector, Tura—Tagil interfluve, west of well 1482 (from the collection.of V..5.Penzgner,. 19/53) Quaternary deposits 0.0 — 3.4 Grayish brown-brown, sandy loam with numerous frag- ments of eroded gaize underlain by sandy loam. Serov suite — Pg} 3.5—13.2 m Light gray to gray, solid, lightweight gaize with rough, subconchoidal fracture, micaceous in places. Talitsa suite — Pg, 13.2—17.5— Muddy gray, silty argillite with laminar accumulations 24.0 m of siltstone with mica; lower the argillites are lighter colored and poorer in siltstone, in places slightly gaize- like (probably diatomaceous argillites). Core is inter- rupted. 24.0—26.5 m Diatomaceous, silty, gray (when moist), micaceous, light clay. At end of stratum there are laminae of light gray, micaceous siltstone containing grains of glauconite under- lain by an interlayer of glauconitic-quartzy, light gray, slightly cemented, micaceous sandstone. Lamination is horizontal, vaguely horizontal in the diatomaceous clays. 26:5— 31.0 m Typical Paleocene muddy gray and dark gray, finely foliated, silty, micaceous clays with laminae of diatoma- ceous clays analogous to those described above. 31.0—48.0 m Gray, diatomitelike argillite splits into smooth plates. At 43.3 m occurs an interlayer of fine-grained, glauconitic sandstone. Siltstone witha large amount of mica and single grains of glauconite occurs on the planes of lamination. 48.0—51.0 m Fine-grained and varied, glauconitic, micaceous, mono- lithic sandstone, in places pierced uninterruptedly by dark gray, argillaceous substance. Lamination is vague. 51.0—63.5 m Gray, muddy gray, micaceous, dense argillite often with accumulation of silty matter with mica and glauconite on the planes of lamination, which are vaguely horizontal. Remains of herbaceous plants are encountered. Downward the rocks become richer in sandy and glauconitic material. Slavgorod suite — Cr," *"°P 63.5—65.8 m Light gray with very slight greenish tinge, argillaceous, micaceous diatomite with inclusions of silty matter con- taining glauconite. The rock contains fish teeth, pyritized and carbonized remains of herbaceous plants; the rock is easily soiled and indistinctly laminated. 107 65.8—69.0 m Gray to dark gray, firm, dense, micaceous, silty gaize with frequent accumulations of sandy-glauconitic and quartzy material with sparse quartz gravel. 69.0—77.5 m Fine-grained, gray to light gray micaceous-quartzy sand- stone with glauconite and only moderately cemented and vaguely laminated. This stratum is underlain by variously colored kaolin clays of the Lower Cretaceous. Three samples from well 1503 (no. 15, 64.0 m, Slavgorod suite; no. 5, 25.5 m, and no. 9, 40.0 m, Talitsa suite) were examined. Only rocks of the Talitsa suite contain diatom and silicoflagellate remains. The diatom complexes of the lower and middle parts of the Talitsa suite are quite similar (Table 21) and differ mainly in the numbers of individual species. For example, frustules of Stephanopyxis ferox (Grev.) Ralfs, S.lavrenkoi Jousé, Triceratium weissi Grun. and Trinacria pileolus Ehr. var. pileolus are less numerous in the upper sample where T. regina var. obtusa Witt. is more abundant. This complex is analogous to the Early Paleocene flora of the eastern slope of the Urals, which resembles the older complex in poor development of silicoflagellates and lack of Hemiaulus polymorphus var. frigida Grun. and Triceratium heibergii Grun., and the younger complex in the high development of Stephanopyxis lavrenkoi Jousé, and S. ferox (Grev.) Ralfs, and the low density of Trinacria pileolus Ehr. var. pileolus. Both samples show a similar, fairly uniform and quantitatively modest silicoflagellate flora (Table 21). The genus Dictyocha triacantha Ehr. is represented by 4 varieties; there are also isolated skeletons of Vallacerta hortonii Hanna, Dictyocha archangelskiana (Schulz) Gleser, D.furcata Jousé and Mesocena aff. apiculata (Schulz) Defl. : Basin of the Bol'shoi Aktai The silicoflagellates of this basin were examined in preparation 21 of the dried diatom collection of MGU. This diatom complex has been placed in the Upper Cretaceous. Judging from the species composition designated on the tag of the preparation (Table 22), this complex is analogous to the Santonian-Campanian of the eastern slope of the Urals. The silicoflagellate flora is relatively varied and abundant. Lyramula furcula Hanna and 2 species of Vallacerta Hanna — V. hortonii Hanna and V. simplex Jousé — appear in considerable amounts; Cornua trifurcata Schulz is frequent. Dictyochaceae are represented by only 2 forms — Dictyocha triacantha var. apiculata Lemm. f. apiculata andf. late-radiata Schulz — whose skeletons occur in small amounts. In the basin of the Poludennyi Aktai, Belaya Rechka village (preparation no. 45 of the dried diatom collection of MGU) the Upper Cretaceous (Santonian-Campanian) diatom complex is accompanied by 5 silicoflagellate species (Table 22) of which 4 species belong to the families Vallacertaceae 108 ‘unId) DdafiuIiDI DIaYI0L9} J ‘UNIN v]JaZUOPO WNI9aY7201U0F ‘asnor snnbiqup * yy ‘asnog snoMjawuhsn * *TOSOTD if (zjnyos) vunrysjasunyouv Dy20/j91(7 ‘asnof snzpjnuiysa “yy Z *Z[NYIS vypIANf{I47 DNULOD ‘asnof s7us0922a I ‘euuey raydwis “7 | uetueduied -alg ‘IRA wnsourshoahjod snjnviwa py aSeyTIA eyYOoY bd “euuey] vpnoun{ vpnwoshT nines “11Z)NYyos eee ek J “BUURET 21U0j10Y 17L99D]]0 4 : ‘IeA ‘UIOIG 11zZ7nNYIs sixidouvnyda,y Bad. Tes Tey qeUuaeN IO” Cy *z]NYIS Zz DIDIPD4-a}D] “J DIVINIIdD “IBA *} “CT ‘pDypjnoidp *} “WIWaT vyD)NI jt ~dp ‘1eA vyquvonI4, = vyr0hj21q7 ‘asnof vasnjasa vppIThg ra ‘Z[NYIS vyvIuNfi47 DNULOD ‘aSNOL apaowIss1UD VIMIDUI i ‘euuRyyT raydwis “7 ‘OSNOf S271gQDLIUW D1YZIAL0q G ‘euuey, vynoun{ vjnwosh'T ‘gsnor 2z7NYyIs wNI7ID4992I4 J G ‘asnor zaydwis ‘A uequeduied ‘gsnof DaIvjad9 “IRA YO 1IZ]NYOIS c ‘eUURT]T 22uU0j10Y 074990]]0 4 -uetuolues | “IRA ‘UI9}S 22z7NYIs sizidouvydayg JOATY TeV TOYS, 10d 1% uollen[eAa 2ATleitquenb satoads PIOT} satoads wo1e Ip jo asVy ‘ou Aqtyeo id taki uotlviedaig SOIP[[ISETJOOTIS soxotdwiod WOIIP OTIsTISIORIeYO (MOW Jo uondeT{oo aya woj) s19ATI Tey ThuUapnjog pur TeIAY JoYs,[og ay1 Jo uTseq a Jo syfsodap snosdFIaID WOY sotduies Jo uoTeUTUIeXa DIdOdSOIOTUI Jo syNsoY *ZZ ATAVL 109 04 Defl. and Cornuaceae Gem. and one species to Dictyochaceae Lemm. All the silicoflagellates appear in limited numbers. Alapaevsk area Core samples from a number of wells (31, 36, 73, 130) bored north of the town of Alapaevsk were examined. Algal remains were found only in the core of well 31. Of two samples from the diatomite layer of the Serov suite analyzed (no. 4d, 7.5 m; no. 4, 6 m), only the latter contained algal remains (Table 23). Mass development of forms of Melosira sulcata (Ehr.) Ktz. and the very frequent occurrence of Anaulus weyprechtii Grun. and Eunotogramma weissii Ehr. indicate that this complex is analogous to the Early Eocene flora of the Lower Ob. Together with remains of the Early Eocene diatom flora a relatively varied silicoflagellate complex of 12 species, varieties and forms of the family Dictyochaceae Lemm. was encountered. Dictyocha fibula var. fibula f. eocaenica Krotov and 2 varieties of D. lamellifera Gleser are dominant; D. deflandrei Freng. var. deflandrei, D. elongata Gleser and Naviculopsis robusta Defl. are rare, and the remaining species very rare. Koptelovo area Cores from 2 wells (232 and 255) situated north of the town of Koptelovo (from the collection of V.S. Pevzner, 1958) were examined; only one of these (255) showed evidence of fossil algae. Well 255 Quaternary deposits 0.0—8.6 m Brown and gray clays and loams overlie the eroded surface of light gray siltstones. Irbit suite — Pg3-3 8.6—10.0 m Silty, weathered, gray to light gray diatomite; grains of quartz and glauconite are encountered. Serov suite — Pg} 10.0—11.5 m Gray to dark gray, firm gaize with numerous nodules and pebbles of black phosphorites with accumulations of sandy and gravelly glauconitic material. 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[ eruor ee : ee tal siisodap OUT Bre eiukpeyy hutod) if Djajdwod "IvA radpuvjfap vyI0hj,01(7 dno13) *zyy (‘Ayy) DIVIINS D«ISOjapy auasoz[ed aytpeziey| eAeXupolsir/eoz Z ‘Jaso[) (Z[NYOS) wow2w “IRA “G “AJ ‘pDyppnaidvig “IeA “BUdIY J ‘(Wuay) v7D7NIIdD1q sisdojNI1av Ay ‘Z[NYIS s0UIUW qo jo J ‘J Dyvjnoidp ‘iRA vYyjJUvIDIA] ‘d ms ym eam z Tod vuojisuvs, “CT H ‘A (unig) vjpwwa? pj}a1m0UNLy jorseoo | (egg c ‘DIDPUNIOL “IVA ASNOL VDJDpuNzod *(T ‘yW10q yo ‘dway s710v42 vppixhig ‘eikpeyry “408 ender ‘IY Snywipps +9 susodap ekeKupais qutod ) -8]) V}4a0U1 "y Siquasva ‘IRA *f “7 ale] ‘und vjajdasqns “tea ‘d “9g | ouasoated Ae[D| Jo yueg yotle/ses uo] uot -enyeaa -enpeaa sotoads PIO sotoeds ‘ou a ae tu01eT a te asy ASojouat Ayqzeoo7 | etd -tuUenb +P -tquenb Tous H jo o8y -WleS $O1LT[2B ETJOOTLIS Saxd[dUIOD WIOIkIp OTIsTIBIOeIeYO (penutiu0d) 9% AIGVL 115 (109) -en[eAo 3AnTle} -Tluenb ‘pyojnoidvig “IeA “Budly (‘uway) v707nNI1dn1q_ sisdopnoian Ay “IOSO[D) 4OUIW "J SIU49UI “IRA “7 “WUlo'Ty DI]DISDY “IBA DYJUDIDIA] ‘Dd af1]] aun) ‘IRA JaSa[H véafijjauvy vyI0/}791 ‘pyvjnoidpiq “IeA “BUILT es dé) MT (wway) vzp7nI1dn1q sisdojnoiav Ay ‘DYJUDIDIA] “J DYJUDIVIAZ “IVA “AY DYJUDIDIA] $1]UALDI “J “LOSOTH $27 —UadDd “IRA 11)jansuat{ DYI0AZI1 1d 1 ‘IasaT) (z[NyoS) sowiw “eA “Gg “Ay ‘Dypjnoidvig “ieA ‘“SUdIy (‘wulay) vyn7nNI1dv1q sisdojnaav Ay “IOSO[X) 4OUIW “"} SIW4aUI “IRA “7 “Z]NYIG sourw ‘J Dypjnaidp "1eA DYJUDIDIA} sotoads SA1e[ [eB PYOOTIS aD GL auac04 Ayreq aus004 (2) ®IPPIW auss04 (0) 21pprw uot -enyeAd aATle1 -nuenb PIOYJ wo1eTp jo o3y ‘IYY 118sian vuwwossojoun gy ‘unity 227YI9a1dham snynoup ‘WO vIIssna vIpIxfidopnasg ‘Ss "YW wnsojnd14]Uaa “7 “SY MayUuryY WN17ZD49II4 T ‘asnof sisuappan *9 ‘undIny snsod -0O49DU "IBA 142]]20U SNIS1pOU1I80j *(sur0j Jo dnoz8) = sy[ey (‘uly Jo ‘Aad) Si4un7 sixAdounyda > *(SUIOJ JO dnoi8) *zyy (ayy) vVI]Ns vsIsojapy ‘HA (uns) vjpwwas vjjaImounsy ‘asnof sisuappun *Q ‘unin) snuod -O4IDUW “ABA 149]]00W SnIsipoU1Iso) *(suroj yo dnoi8) syjyey (‘ULY Jo *AOID) S24477 sixidouvydag *(SUIIO} JO dnoi8) *zyy (‘1yq) VjDI]NS v4iSOjapYy ‘HA (undid) vjpwwas vjjaimounsy ‘asnor sisuazpin “9 ‘und snuod -OLIDUL “IRA 149]]20U SNISIPOUIIS0) satoads saxa[dulod WIOIeIp IIsTIBNIOeIeEYD susodap auasoa[ed sitsodap auaso0ateg s1isodap auasozied piXpeyy eXeku pais pure eXeku -UNI2A | (102% ayi to futod) aANTJIFIUIIZ/ 10% eidpeyy eXeku pois pue ekeku Aeyo -yI2A | (T0z snosoe ayijo futod) -WoieIq | PNT}I21UI/T/ 10% wary | (G0z eikpeyy futod) eXeXupals|t/S0z ‘ou A8oqouary | Aatpeoo7 | aqd (panutiuoo) 93 AIGVL 116 110 Two samples of the Irbit suite diatomite from the 8.6 —10.0 m interval (no. 1 — upper; no. la — lower sample) were examined. Remains of diatoms and silicoflagellates were found in both samples (Table 24), but are more numerous and better preserved in the upper sample. Very numerous are Melosira sulcata var. siberica Grun., Stephanopyxis turris Var. intermetdra Grun., Coscinodiscus moelleri vari m aero. porus Grun., Hemiaulus polymorphus var. frigida Grun. et var. morsianus Grun. and Goniothecium odontella Ehr. var. odontella; however, most of the species are represented by isolated or rare specimens. Such a systematic composition of diatom flora indicates an Eocene age, although an exact determination is difficult. In the other sample (no. la), only Melosira sulcata (Ehr.) Ktz. (group of forms) and Hyalodiscus sp. (umbilicus) are encountered in large numbers; the few other species are represented by single specimens. The silicoflagellates are also more abundant and diverse at a depth of 8.6 m. Of the 9 species, varieties and forms, Dictyocha lamellifera Gleser var. lamellifera and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata are abundant. Other forms — N. biapiculata var. minor (Schulz) Gleser, Dictyocha elata Gleser var. elata and D.ftrenguellii var: .carentis Gleserf..carentis —.occur rarely, and the remaining 4 forms very rarely. In the lower sample there are isolated skeletons of 3 forms appearing at higher density in the upper sample. Kurgan Region Weil 2; Ust"-Uiskee village, Duyvyanius profile (from the collection of Vp: "Pevenery 19 53) Quaternary deposits 0:0 —8.5-m Fragments of diatomites and gaizes with quartz gravel. Chegan suite — Pg3— Pg} 8.5—49.5 m Sandy clays, often similar to diatomaceous clays. Lyulimvor suite — Pg}~3 49.5—132.0 m_ Tripoli (diatomites?) with siltstone containing diatoma- ceous material above and diatomaceous, often sandy gaize below 107.5 m. 117 Talitsa suite — Pg, 132.0—139.0 m_ Silty, muddy gray clays. Gan'kino suite — Crj” 139.0—208.0 m Mealy, light gray to white, dense marl. Slavgorod suite — Cr," "°P 208.0—263.7 m Argillite — gaizelike, rarely tripolilike; argillite; glauconitic sandstone at bottom. Microscopic examination of a sample from the Lyulimvor suite (99.0 m) revealed algal remains in a rather poor condition (Table 25). There were numerous frustules of Melosira ornata Grun., Stephanopyxis turris var. intermedia Grun. and Pseudo- pyxilla russica (Pant.) Forti. The presence of some species of Coscinodiscus, although in limited numbers, together with the occur- rence of isolated valves of Melosira polaris Grun., Stephanopyxis marginata Grun. and Pyxilla gracilis Temp. et Forti indicate that this complex belongs to the Late Eocene. The silicoflagellates are not numerous ( 8 species, varieties and forms). Most abundant are varieties of Naviculopsis biapiculata (Lemm.) Freng.; there are rare skeletons of Dictyocha frenguellii var. carentis Gleser f.carentis and very rare ones of D. rotundata Jousé var. rotundata, D. fibula Ehr. var. fibula f. fibula and 2 forms of D. triacantha Ehr. Thus, the following silicoflagellate complexes can be distinguished on the eastern slope of the Urals and Transurals: Santonian-Campanian, Early Paleocene, Early Eocene, Middle Eocene (?), Late Eocene, Late Eocene — Early Oligocene(?), and Early Oligocene (?). West Siberian plain Southern part of Taz Peninsula (from the collection of F. A. Alyavdin) Interfluive of the Verkhnyaya and Srednyaya Khadyta Point 201 Two samples of clay were examined. Both contained diatom and silico- flagellate remains (Table 26). In view of the abundance of Coscinodis- cus uralensis Jousé andC. moelleri var.macroporus Grun. 118 112 and the absence of other species of Coscinodiscus, the complex found in sample 1 can be placed in the Middle(?) Eocene. Very few silicoflagellates are encountered here: there were only 3 isolated forms — Drctyocha triacantiha hr. yar. triacantha f. triacant he, D. irenguelliil var. carentis Gleserf. carentis, and Naviculop- sis biapiculata (Lemm.) Freng. var. biapiculata. The diatom complex of sample 2 is of a different character. The abundance of Anaulus weyprechtii Grun. and occurrence of single frustules of Coscinodiscus uralensis Jouse makes it comparable to the Early Eocene flora of the Lower Ob. However, the complex does not include Triceratium mirabile Jousé —a highly characteristic Early Eocene species known from the contemporaneous deposits of the Lower Ob area and the eastern slope of the Urals. The silicoflagellate flora of the second sample consists of Dictyocha lamellifera Gleser var. lamellifera (rare), 2 varieties of D. triacantha Ehr. and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata (very rare). Basin of the Srednyaya Khadyta River Point 203 One sample was examined from the middle part of a 30-m layer of Paleogene clays underlying Quaternary sands and loams. Numerous, well preserved algal remains were found (Table 26), including considerable numbers of varieties of Melosira sulcata (Ehr.) Ktz. and Stephano- pyxis turris (Grev. et Arn.) Ralfs,as well as Coscinodiscus argue Ehr.C.polyactics, A.Cls and Pyxilla ipracilis Demp;..et Forti. This complex, led by T. gracilis Temp. et Forti, can be placed with reservation in the Late Eocene—Early Oligocene. Stratigraphically, the complex occupies the lower part of the Chegan suite. There are only 5 silicoflagellate species with 7 varieties and forms. Dictyocha rotundata Jousé var. rotundata dominates the complex, although D. rotundata var. secta Gleser and D.transitoria Defl. are also represented by a considerable number of specimens. The remain- ing silicoflagellates occurred as rare specimens. Point 205 Examination of a sample of Paleogene clays from a 4-m outcrop revealed a diatom complex analogous to that of sample 1 (Table 26) from the interfluve of the Srednyaya and Verkhnyaya Khadyta rivers (point 201), and can likewise be placed conditionally in the Middle Eocene. The silicoflagellate flora consists of 4 species with 6 varieties and forms. Two forms belonged to Dictyocha triacantha Ehr, 2 varieties to Naviculopsis biapiculata (Lemm.) Freng. All the silicoflagellates are very rare, except Dictyocha lamellifera Gleser var. lamellifera whichis rare. 18 Guli of ‘Ob coast. the: Vere Dank’ ot (the Srednyaya Khadyta Point 335 A sample of Paleogene clays from the lower part of an outcrop beneath Quaternary deposits was examined. The clays are dense, coarse- fragmented, yellowish gray, greenish when dry and bluish when moist. The abundance of valves of Melosira sulcata (Ehr.) Ktz. (group of forms), Coscinodiscus payeri Grun. var. payeri et var. subrepleta Grun., C. radiatus Ehr., andGrunowiella gemmata (Grun.) V.H. indicates that the complex belongs to the Late Eocene. Dictyocha rotundata Jousévar. rotundata and D. frenguellii var.carentis f. incerta Gleser predominate among the silicoflagellates; the remaining species and forms of Dictyocha Ehr. and Naviculopsis (Lemm.) are very rare or rare (Table 26). To sum up, the diatoms of the Early, Middle (?) and Late Eocene and Late Eocene — Early Oligocene (?) of the southwestern part of the Taz peninsula and the interfluve of the Verkhnyaya and Srednyaya Khadyta are accompanied by silicoflagellate complexes of the same ages. Basin Jof tine Kinabinruttia Hives One sample (no. 6 from outcrop 31) of brown sandy clays alternating with thin sandy interlayers was examined microscopically. The sample came from the middle reaches of the river. Upon drying the clays become light-colored and split into separate plates. The clays form a dome on the scarp of the original bank and sink below the waterline; their visible thickness is about 8—9 m. The sample contained a very uniform complex of poorly preserveddiatoms (Table 27). Dominant are Pyxilla gracilis Temp. et Forti, P. oligocaenica Jousé var. oligocaenica et var. tenuis Jousé, Pseudopodosira bella Possnova et Gleser, and Melosira sulcata var. siberica Grun. The abundance of Pyxilla oligocaenica var. tenuis Jousé makes this complex analogous to that from the Pelym River basin (Burmantovo profile) and it can be placed conditionally in the Early Oligocene. The Khabirutta complex was apparently associated with shallower waters since it lacks species of Coscinodiscus Ehr. This assumption is also supported by the abundance of sandy material in the rock in which the algal remains are found. Silicoflagellates are rather abundant here (Table 27). Dominating are Distephanus antiquus Gleser, Dictyocha elata var.media Gleser f. media et f. reducta Gleser, D. rotundata Jousé var. rotundata and D. spinosa (Defl.) Gleser. There are smaller amounts of D. frenguellii var. carentis Gleserf.carentis, D. rotundata var. secta Gleser, etc. 120 TPC | spuawa “AG podijja DvUaISa fy C Jasayy smmbizuv snuvnydajsiq ‘pyppnaidpig “ABA “BUA J (;wuto’{) pyppnoidvig sisdo]ng1av AJ “ZpNYOS Louru | a pyppnoidy "AtA DYJUBIDIL] “CT Z ‘Tod vioyisund? °d € ‘Waso[D vjIas “ABA “YG y ‘pippunjod “IRA QSNOL DIVPUNJOL “CT y ‘asopy (Yad) vseurds “q “das J -O[) Dpdaoul “Jy S]]UIdVI “ILA Meas "S1]UadDd "| AAS € -a]) Suadvo “ARN iipponduad~ “Los 0) OJ) vjanpas "y DJpau “AVA *A Tah ‘pip Cc -au "J dasayy) vipamw “IBA VIV}9 “CT ‘pjajdwod "J daSo|x) Y)a7dwor | “MA ‘“Buatg rapupjfap vy0h}21q uoll -eny[eAd dATIVI -Tluenb satoads (2) aue9 -0811Q Aqirg RIOT] WUO1eIP jo a8y ‘asnog sinuaz “ABA Ya YI!UADI -o#1)0 “ABA QsNof vI2UaDI0TI}0 ‘d ‘dog ja “dway, sipvss ppprhd (snoyiquin) ‘ds snosipojviy “Laso] 9 9 vAOUSSOg 0]/9q v4ISopodopnasd UNI) DoIdAgIs “ABA DIDIINS “WV ‘unIy déasan]I D41S0]9W suisod shepo Apurs umoig 9 onmw mow -ap auasoe[ed uoll -enyteAd satoads ‘ou aAt1v1 a ' ‘oO I 3 -tquenb jouNT I -wes SOP TTIBeTJOOMTTS soxatduiod woirip oTIstI919PIeYD (uiparkTy “VY ‘4 JO uoTIDaTTOO 9y] wodj) PlINIIqeyy 113 ayi fo Ulseq oy UT TE dossino Woy opdiues e JO UoOTeUTWIe XS ddoososottu jo synsoy “LZ ATAVL 121 114 Basin of the En-Yakha River Point 21 On the right original bank of the En-Yakha River 3.5—4.0 km above the mouth of the Titin- Kalovy-Yakha stream, the outcrop is 16—17 m high; in the central part it is 22 m above the waterline and its length is 450 — 500 m. In the central part of the outcrop, blue and bluish green clays emerge to a height of 9—12 m from the waterline; these are overlain by dark gray sandy clays. Further downstream a landslide uncovered light brown (green-tinged hue when freshly cut) sandy clays with parallel lamination at an angle of about 20° to the horizon. The thickness of each stratum ranges from 1.5 to 3.5 m; they are separated by very thin "yrisypki'' of gray, fine-grained, slightly micaceous sand. In the talus, the clays form a fine, laminar scree of light gray color when dry. Clay sample 21/4. Between these and the blue clays emerge clays from which sample 21/5 was taken. In the low part of the upstream end of the outcrop emerge sandy, horizontally-obliquely laminated sediments with laminae of brown clay. These sediments gradually pass into splintered clays with ferruginized surface. On clearing these clays, a fragment of carbonized wood was revealed. F.A.Kaplyanskaya noted siderite loaves in the cleared clay. These clays can be placed in the Chegan suite. Clay samples nos. 21/1, 21/4, and 21/5 from this outcrop were examined. A single type of diatom flora was found in all the samples (Table 28). The most varied and well preserved complex was found in sample 21/4. Here are numerous valves of Pyxilla oligocaenica var. tenuis Jousé, P. gracilis Temp. et Forti, Coscinodiscus decrescens Grun., Brightwellia hyperborea Grun., and Melosira sulcata (Ehr.) Ktz. (group of forms). Sample 21/1 contains a numerically more modest complex, and sample 21/5 a very poor complex. The observed diatom complex is analogous to that from the Pelym and Khabirutta rivers, which was placed conditionally in the Early Oligocene. A total of 16 silicoflagellate species, varieties and forms were found. Dictyocha elata var. media Gleser f. media etf. reducta Gleser is most abundant in all samples. Distephanus antiquus Gleser is dominant in 2 samples; in addition, sample 21/1 contained numerous Skeletons of Dictyocha rotundata var. secta Gleser, and sample 21/4 Naviculopsis biapiculata var. minor (Schulz) Gleser. Sample 21/1 contained a relatively large number of skeletons of the rare species Dictyocha spinosa (Defl.) Gleser; another rare species in the Paleogene is Mesocena elliptica Ehr. emend. Defl., whose skeletons were found in 2 samples. The remaining silicoflagellate forms are very rare or rare. Point 23 Right bank of the En-Yakha River. Anoutcrop, 6-7 mhigh, 175—200 m long, situated 10.5 km below the mouth of the Kho-Yakha stream, a right tributary of the En-Yakha. 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“ABA DIIUavI0TI0 “dq ‘tog yo “dway $1729043 vjpizig “(quaw8ey) ‘ds snosipopviyy *(suIOJ JO dno3B) *zyy (ay) VyVIZNS vuISOLa PY :jo Ajuo Sutistsuoo ‘addy SUES DY JO PIOTJ paystIeAod ut ATYSIH ‘asnor simuaz “4eA DI1UavI051]0 *q ‘Woy «yo “duwioy, s2729013 vp Tig ‘unig, vasoguadhy v17,aN7Y314 gq satoads soxatdwiod WOIeIp dTsTIAIOvIeYD sitsodap auaso0eated susodap auasoated sisodap auasoe[ed Aeqo Kew ystnta ¢/€z skeTD c/1z Keyo pesun -uaels ‘UMOIq 181] ‘Apues HV wi ‘yidaq} otd -uwIeS ASojouary (panunuos) gz AIsVL 124 5698 aAIN wD coin tO OD on if (117) ‘rasoyQ (zpnyos) 1ou2w “AeA *Q “N ‘pyojnaidpig “ied “Buddy (‘uuaeTy) 0707nI1d01q s1sdo]n910D NY “Jasa]) Loulw “y swiaur “Jed “7° “UWA DIVISDY “ABA? “CT “ZNYOS s0urw ‘| vypjpnaidp “IRA vyJUDIvIAT “CT "TOSI VjIaS “ABA “A “CG “D]Dp -unjot ‘IBA osnof DyJDpUNzOL “CT ‘piaf -1]]9WD] “TWA JaSa[ VLIfI]]aWV] “J “10S -O[) Dj4aaur “JF S7ZUaLDI “IVA Le @ *S1] -Uaivd *} JOSa{H Ssyuaiva “er “f{ “CT 12] -janSuaaf “AVA “[Joq AMjansuaif *q ‘pyvja “TRA Josey B7vJa vYyI0/}21q aus004 21e7 ‘rasapy (z[nyoS) sowzw “ABA “q “N ‘pyojnaidvig “ABA “SUdIY (‘wuley) 2707NI1d02q s1sd0)n920D AJ [fod Pio0jsuns) °C (2) auao ‘rasop (‘Jod) vsourds “q -08110 “JOSIJH YjIAS “AVA “4 “CJ Ayrea ‘DIVpUNIOL “AVA BSNOL VJVPUNZOL *(T - 909904 “2pjansuaif ‘IeA [JOM wpansuasf vyvohj01q aie] uotl -enjeaa satoads PIO ane w01e1p -tuenb jo sy $d1P[[ABeTJOOTTIS "HA (unin) v7pwwas vjjaimounsy wWnIzDsLaIIA I “IG SNpVIpvA ‘uahvd “aed “unig qahvd *9 ‘unin sniod -0O19DW “LWA 149]]90Ul SnIS1po0Uu19S0) *(suz0j Jo dnois) sey (uty 4a “AorID) si4unz “Ss sivfiidounyda}g *(SUIIOJ JO dno18) *z}y (aug) 07DI7NS vAIS UNIDULOLA Aeyo uMoIq ystXein|yueg styl | /eyz auaso2[ed auasoeted soxa[dwiod woleIp OTstIaIoRIeYD -wes (penuyuos) gZ aTAVL 125 (118) —_ oO) se | oD wo co S € uoll -en[PAd aATIeI -Tluenb “JOSOPH (zpNyoS) sowrw “eA “q “NV ‘pyvjnaidnig “1eA “BUILT (‘uuoy) v7npnI2dv1q sisdojnajav Ay “Z[NYIS ‘} Dyvjnaidp “IeA "2 “Gf “DYJUDIVDIA] “| DYJUDIVIA, “ABA “IYY VYJUVIDIAZ “CG Jour “D4af i] -J9WD] “IRA JOSI[) VLaf1q]9aWY? 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The clays are bluish gray and gray. One sample from these clays (no. 23/3) was examined. It contains abundant, well preserved algal remains (Table 28). Considering the abundance of valves of Pyxilla gracilis Temp. et Forti and the considerable amount of frustules of Brightwellia hyper- borea .Grun.j (Coscinediscms argus hr., and Cc. mirabilis Jousé, this complex can be regarded as analogous to that from the top of the Lyulimvor suite and the bottom of the Chegan suite, and thus probably belongs to the Late Eocene — Early Oligocene. 119 The silicoflagellate skeletons found here belong to 14 species, varieties and forms. Dominant are Dictyocha rotundata Jousé var. rotund- ata et var. secta Gleser and Naviculopsis biapiculata var. minor (Schulz) Gleser. D. deflandrei var. completa f. producta Gleser and D. fibula Ehr. var. fibula f. fibula are common, and D. deflandrei var. bicornuta Gleser, D. frengu.ellii var. carentis Gleserf. carentis, D.transitoria Defl. and Naviculop- sis biapiculata (Lemm.) Freng. var. biapiculata are frequent. The remaining silicoflagellates are less numerous. Point 24a Right bank of the En-Yakha, above the river mouth. The outcrop reveals a cross section of a ridge about 6 m high. The central part of the ridge consists of fine sandy diatomaceous clays which are almost white when dry. Microscopic examination of a sample (no. 24a/1) of these clays showed the presence of diatom frustules and silicoflagellate skeletons. The characteristic diatom complex (Table 28) consists of typical Late Eocene species of the West Siberian plain andthe eastern slope of the Urals. Twelve species, varieties and forms of silicoflagellates were deter- mined. Most abundant are Dictyocha frenguellii var. carentis Gleser f.carentis andf. incerta Gleser and D. rotundata Jousé var. rotundata. The remaining species are very rare or rare (Table 28). Point 25 An outcrop, 7—8 m high, situated on the right bank of a small stream joining the Khadutte below the mouth of the En-Yakha. The section shows a ridge directed northeast. The Quaternary deposits in the form of gray quartz sands on the top are underlain by grayish brown— gray, sandy Paleogene clays of fine cloddy structure, which become light-colored on drying. The clays evidently continue below the waterline; their visible thickness is about 5.5 m. One sample (no. 25/1) from the clay of this outcrop was examined. The sample contained rich diatom and silicoflagellate remains (Table 28). 127 120 The main characteristic of the diatom complex of this sample is the abundance of Coscinodiscus uralensis Jousé in contrast to the much smaller density of C. moelleri var. macroporus Grun. On these grounds the complex can be correlated with the Middle (?) Eocene flora to the West Siberian plain. The silicoflagellate complex consists of 8 species, varieties and forms. Dictyocha frenguellii var.carentis Gleserf. carentis and Naviculopsis biapiculata var. minor (Schulz) Gleser are dominant; Dictyocha lamellifera Gleser var. lamellifera appears in somewhat smaller amounts. The remaining silicoflagellates are very rare or rare. Point 27 Outcrop situated on the right bank of the En-Yakha, 1 km below the mouth of Titin-Kalovy-Yakha, a right tributary of the river. The precipice is 18—20 m high and about 1.5 km long. The outcrop slopes are covered with landslides. Clay deluvium emerges in the small beds of the streams. Examination of a sample (no. 27/1) of these clays revealed well pre- served algal remains (Table 28). The table shows that the dominant diatom complex includes only 2 Coscinodiscus species — C. moelleri var. macroporus Grun. andC. uralensis Jouse. This is characteristic of the Middle (?) Eocene diatom flora. There are 8 silicoflagellate species, varieties and forms. Two of these — Dictyocha frenguellii var. carentis Gleserf. carentis and Naviculopsis biapiculata var. minor (Schulz) Gleser — are very abundant. The skeletons of Dictyocha lamellifera Gleser var. lamellifer'a, D. elata Gleser var, elata, D: trhacentha var. apiculata f. minor Schulz and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata are frequent. Thus, the algal flora in the basin of the En-Yakha belongs to the Middle (?) and Late Eocene, the Late Eocene — Early Oligocene (?) and the Early Oligocene. Basin of the Arka-Tab-Yakha River Point 14 The outcrop lies 1.5 km south of the northeast bend of the Arka- Tab- Yakha on the shore of a lake. The precipice is fairly steep, 7—8 m high. The upper part of the outcrop consists of sandy, dark brown, laminated clays. Downward the clays merge gradually with lighter-colored, fine- cloddy sandy clays which continue below the waterline. From the west, the clays are joined at an angle of about 75° by fine, sandy, greenish gray clays which also extend below the waterline. The following samples were examined: no. 14/1 of the dark brown clays, no. 14/2 of thelighter-colored clays, no. 14/3 of the greenish gray clays. 128 (121) *S1} ~Uaivd *} TOSa[t) S77UasDI “AeA *f *G 121 ~janSuasf “IeA “[Jaq mMpjensuasf *q ‘D]D]a “AVA JASE) 27D}a VYI0/}21q "Jaso[X) (Z[MYOS) sou2w “IRA “q “AN ‘pippnaidviq “eA *SUALT (‘urtaey) vyvjnII1dv1q sisdojna1av NV “WUT VzVISDY “ABA *} *G ‘Z[NYIS sourw ‘} Dyopnaidp “IeA vYyzUDIVIA? °C “DJVPUNJOL “AVA YSNOL DJVPUNIOL °C] “D4afi] -]9WD] “IBA JOSITH vsf2}]aWDv] *G “49S -8[) DjLaIUI “} Si7UaDI “IRA *f *G *S1] -UdLDI “J LOSI[X) S27UaLDI “IRA “f° "12018 -nguasf “IeA “[Joq Wpjanduasf *q ‘pjD]2 “ABA JaSa[ 2IDJa vYyI0h}21q uoTd -en[PAd dATIEI -tquenb satoads SOIL [AB LTJOTTIS *(suisoj yo dnoss) sj[ey (‘uy 49 "AOID) s244n7 sizidounydazg ‘(snorjiquin) ‘ds snosipopvhiyy “UnID, DIDULO * *(sulIO} JO dno13) *zyy (ayy) 27DI7NS D41180]9 W aus904 ({) aT PPI C ‘ysny (qley{) v7djnara vI490UI4 J ¢ "ADIN, WNJVULOLA WN14DL9914 J V4 ‘gsnof szsuapvun *9 v7 “IY SnzDIpvs *D y ‘waahvd “IeA ‘unig tuahvd “9 ‘unin, snsodos -DW “JRA 24a)]20W sSnIsipoU19so) ‘asnor vjipjaund *¢ ‘asnor vypa sixidouvydazg *(suJO} jo dnoi8) *zyy (ay) 27v9]Ns DuIS0]a ud st od wo soxodwo0d woleIp o1staIORIeYO voll -enpTeAo RIOTS I satoeds dATIe1 woe 1p -twuenb jo ony Aero Apues ‘UMOIG 4Ie Cd sisodap auasoaled susodap Aezo Apues auasooreg] ‘Avis ystuseID “ou ie AZojoyit] jw ‘yidaq} otd (urpardty *y ‘4 JO UOTIDATIOO ay Woy) EYFeA-qeL-eYIY oY2 Jo UIseq ay1 Woy satduies jo stsXteue oIdoososOTUI Jo sNSeY “63 ITAVL 129 (122) NN uoll -en[PAo aATIeI -Tuenb “MoSaTQ (zjNYyoS) «ow “1 "IRA DIVINIIdDIg sisdopNIIAD “Z[NYIS sourw ‘| Dypjnajdv “ARA vYyzUvIVIA] “GQ *$1]UALDI “| dos “OD SljuadvI “RA AIDPJaNduarf “Gq *D]D]9 “APA AOSI[H) VjIN]a vYIOh]21q ‘pDivjnaidpig “AVA “Suds (‘ulute']) v7D)NI2dDI1q sisdojnaiav Ay “ZING s0U -1U *} Djvj)NIIdD “IBA DYJUDIVDIA) “CT *S1]UALDI *}) JOS -9T S17UaLDI “IRA ANjansuasf *q °DID]A “IBA LSA] VIVA DYI0h]}I1¢7 ‘pyvjnI1dvI1q “IRA “Sualy (‘wwaTy) v7VjnI2dv1q sisdopnrnav Ny 3 “bsaf1] -]9WD) “JRA JASI[DH Viaf7jJawD), *q satoods SdIe[TEBeYOOTIS aud004 au9004 (2) 2TPpIW 9u9904 (2) ATpPIN eIOYJ wW101PTp jo any -en[PAd “HA (Cundy)) pjpwwad vjj,a1Imounsy ‘ADIN, WnyvUsOra UnN17D4129I4 J “osnor SISUa]DAN * 4) ‘unity snsod -OLIDIWU “IBA 149]]790W SNISIPOUIISO) “undr) (eIva,O) SnNzPDIpv4 snIsipopv/i TT *(SuIO} jo dnoi8) *zyy (AY) D7VIZNS DuIsOjapy HLA (unig) pjpwwas vjjaimounsy ‘asnof sisuazpvan * 9 ‘uniIn) snuodos -IDU “IBA 149]]90Ul snasipou1Iso) ‘UNI DIpawsaju. “IEA sling “9 ‘unin, my2s01q sixfidouvyda)y ‘(snottiquin) ‘ds snasipojvhiyy *(SuI0} Jo dno) *z}y (AY) VIDIINS viIS0]a WW “10g (UR) DIISSN4 D]ZIZAdop nas gq “UNI, Daafiu1uvI *q “UNIN, Vvaafiaynav vIaY]012)q ‘asnof sisuaypin *9 ‘unig, snusodos -IDU “ABA 149]]20W =snasipoUulIse) sotoads -vuenb soxa[dwiod woleIp o1stisIOeIeYD Aeyo Kea ystusai9 ely) susodap auasoo[ed [ otdwies ut ueya Aepo pasojoo -101431] z/¥t sitsodap auasoe2ed susodap | Aeto Apues auasoeateg| ‘uMoIq yIed 1/¥h ‘ou w ‘yidoq| etd -UWIeS asy ASojouat (panutiuos) 6z ATAVL 130 123 Diatom and silicoflagellate remains were foundinall the samples (Table 29). The table shows that the characteristic complex of the first 2 samples includes only 2 Coscinodiscus species —C. moelleri var. macro- porus Grun. and C. uralensis Jousé. Both species are numerous in the lower sample, while C. uralensis Jousé is frequent and C. moel- leri var. macroporus Grun. very rare in the upper sample. Melo- sira sulcata (Ehr.) Ktz. (group of forms) dominates in both samples, but valves of Pterotheca aculeifera Grun. are very abundant in sample 14/1. The diatom complex of samples 14/1 and 14/2 resembles the Middle (?) Eocene flora of the Lower Ob and Ob— Pur interfluve. Valves of Melosira sulcata (Ehr.) Ktz. (group of forms), Hyalodiscus radiatus (O'Meara) Grun. and Coscinodiscus moelleri var. macroporus Grun. predominate in the sample of greenish gray clay (no. 14/3). All the other diatom species are very rare or rare here. Such a diatom composition suggests the Eocene age of the complex, though a more accurate determination is difficult. The remains of the silicoflagellate flora is fairly scant. Skeletons of Dictyocha frenguellii var. carentis Gleserf. carentis dominate in samples 14/1 and 14/2; in addition, the former sample also contains D. elata Gleser var. elata and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata. Sample 14/3 contains very rare or rare specimens of silicoflagellates. Point 16 The outcrop lies on the right bank of the Arka-Tab-Yakha, 1 km below the mouth of an unnamed tributary. Its height is 12 m and length about 100 m. A peat layer of about 4 m overlays sandy, greenish gray clays with visible thickness of about 8 m. One sample of these clays (no. 16/1) was examined microscopically. The material contained abundant, well preserved algal remains (Table 29). There are numerous frustules of Coscinodiscus uralensis Jouse as well as other species of the same genus such as C. payeri Grun., C. radiatus Ehr.; the predominant forms are Stephanopyxis edita Jousé, S. punctata Jousé, Triceratium exornatum Grev. This complex is analogous to the Late Eocene diatom flora of the Lyulim- vor suite of the West Siberian plain and the Irbit suite of the eastern slope of the Urals. Of the 10 silicoflagellate varieties and forms encountered, high numbers are characteristic of only two — Dictyocha triacantha var. api- culata f. minor Schulz and Naviculopsis biapiculata var. minor (Schulz) Gleser; the rest are scantily represented. Thus, the basin of the Arka-Tab-Yakha contains a Middle (?) and a Late Eocene complex of silicoflagellates and diatoms. 131 127 Eastern part of the West Siberian plain Silicoflagellates were examined in material from natural outcrops on the river Pechal'-Ky, a right tributary of the Taz (the samples were collected by the geologist Kuznetsov). Microscopic examination of 6 samples revealed everywhere the presence of diatom and silicoflagellate remains (Table 30). In almost all the samples, the characteristic diatom complexes consisted of Melosira sulcata (Ehr.) Ktz. (group of forms), Hyalodiscus radiatus (O'Meara) Grun., Coscinodiscus moelleri var. macro- porus Grun., C. payeri Grun., C. radiatus Ehr., Grunowiella gemmata (Grun.) V.H. and others. A similar diatom complex is known from the Lyulimvor suite of several areas of the West Siberian plain and from the Irbit suite of the eastern slope of the Urals; consequently, the observed complex can be placed in the Late Eocene. The presence of significant numbers of Pyxilla gracilis Temp. et Forti insamples 3466 and 3460a-3 does not contradict this conclusion, since this species is not dominant in these samples. The Late Eocene silicoflagellate complex of the Pechal'-Ky River numbers 14 species, varieties and forms. The complex is similar in all the samples, although sample 3466 differs sharply due to the considerable numbers of skeletons of Dictyocha transitoria Defl., which is completely absent from the other samples. The differences between the Pechal'-Ky samples relate mainly to the presence or absence of some individual silicoflagellate forms (varieties and forms of Dictyocha triacantha JEhr:, D. damelliftera Gléser' var. lamelliterar Distephanus speculum (Ehr.) Hack., etc.). Although the silico- flagellates of samples 3503 and 3476 are less abundant than those of samples 3461, 3461-2b, and 3460a-3, the quantitative proportions of the forms within the complex is roughly the same. Dictyocha frenguellii var. carentis Gleserf. carentis andf. incerta Gleser pre- dominate everywhere, while the varieties of Naviculopsis biapi- culata (Lemm.) Freng. occur in smaller numbers. On the other hand, the skeletons of Dictyocha rotundata Jousé var. rotundata are very numerous in the last 3 samples, while in samples 3503 and 3476 this variety is represented by isolated specimens only. Middle Ob area Studies of fossil algae were made of samples from the collection of T.I. Osyko and D. V. Osadchei taken from the well bores in the environs of the villages of Aleksandrovskoe (nos. 2-k, 6-k, 11-k, 15-k), Kargasok (no. 1-p), Vasyugan'e [land along R. Vasyugan] (1-p and 3-k) and Parabel' (Parabel'-Chuzik profile, nos. 7-k, 10-k, 12-k and 15-k). Algae were found in well no. 3-k of the Vasyugan'e profile, and wells 7-k, 10-k and 15-k of the Parabel'-Chuzik profile. : 132 “Zynyag sourw I ‘| pyopnajdp "deA = DYUDIDIA, ‘og yo ‘dway, s129049 npjIthg c “‘pDIvpUNJOL “IBA QSNOL VIVPUNIOL *(T “IW Ssnyvipps “9 *pdaf?] ‘wahvd “ied ‘Und 2Lafhvd +9 } Jawv] “AWA JOSO[ VLef7q]eWv]) *C ‘unin snasod “108 -OLIDWUW “IRA 1.49]]20UW SnIS]po0Uu1IS0) (a -O[) DpLaIU2 “J S17UAIDI “TBA ee OF ‘(stuoy Jo dnows) *s1qua sypey (uly yo “AOID) siuni “g¢ G -DI “J JOSa[H S1jUesDI “IEA We ‘asnof = Dpz1pa sjxfidouvyda)g "1 “ung i (e1eoW,O) snqwipps snasipo) nh yy *(suIO} Jo i ausd0g 218] dnois) *zyy (‘IYyg) 2IPIDNS D4I80]a W’ e—P09PE ‘wnjnoads “IeA *yYOeH l (ay q) wnjnaeds snuvydajsi” } ‘Jasey (zpnyos) sou “IRA *Q “A ‘pyojnaidnig “AeA “SUdA yf ¢ (wwe) 277jn22d01q sisdojns1av Ny ‘HA (unig) ojpwwas vjpajmounsy G [Jo visopsudi? “J ‘tog yo ‘dwey, si2onud vypIehid Zz ‘pippunjod “TWA QSNOL VIVPUNJOL * ) “IYQ SnpDIpv4s “| “10S “qaahod y -O[) Dj4aour “J S2}UaLDI “IBA ea "eA ‘unIg tahvd snasipouissog "s]quaiva “} JOS “(suizoy Jo dnos8) sjjvy Z -O] S2juasva “ABA apjansuatf *d (‘uly JO “AOID) squany sizfidounydalg ‘pjajdwoa "| 1aSo[) 72] *(suIO} jo } -dwos ‘ies jaipunjfap vyI0/h}21q aua00q4 91e7 dnoi8) *z1y (ayy) vjvayNs D.«A18022 99VE uoTien[eAa aateinuenb uoT1en[eAd satoods sotoads RIOT} WOIeTp jo oy aaT eIUENd ‘ou atduires ASojouaty SOIvTLIBETJOOTTIS soxo{duiod WOIeIp STISsTIAIOvIeYD (Aosiauzny Jo UOTIaTTOO ay2 Woy) AM-,[eYIed 9Y1 Jo UIsSeq aYy2 WOT sotduies Jo uoeUTWIeXS dIdodsOIOTW Jo syNSoY “OS ATAVL (124) 133 (125) oO we =o os uollen[ead oat eIUeNb “z[nyos pyppnoidy "aerv "4 "GQ “DYJUDIDIAD “| DYI -UDIDIAY “IRA “AYU DYJUYIDIU? “|G “DIDPUNIOL “IVA YSNOL VJDpUN}OL “GJ “10S -O[D Dj4aIUI “y S1juasvI “ARA “f “Gg Siquatva *f Las “IBA 1Ipjansuasf “Gq JOU "YT -8[9 Sipuasvo ‘pjajd woo ‘f 1ase[9 vjajd “IBA -uloo taipuvjfap vysoh}21¢q “19SO[T) (Z[NYOS) s0W2W “IRA “Q “NV *pypjnoidviq “ARA “BUdL A (ww) vyvpnaidpiq sisdopnoiav iy “WW DIDIsDY “IRA *} °C “ZjnyoS = sour ‘J Dyvpnoidv “ARA vYyJUvIDIA? “Gq ‘DIDPUN}OL “ABA OSNOL DJVPUNIOL * “Jas -O[) Dj1a0U2 “J S2qUelvI “IBA “f “GQ ‘S)] -UaLDI “J JOSO[D S]jUuasps “IRA “f *G 11) -jansuaif “eA “|JOQ Ippansuesf *q “‘Djaydwoo *) Josayg 0727 -dwoo “lea iaipunj{ap vys0hj21q “MOSOTH (Z[NYOS) wourw “AVA “Q “A ‘pjvjnaidviq “RA *BUdIy (wwe) vvnI21dn1q sisdopnaiavN “WUla"] DjVDISDY “ABA “7 “GQ satoeds SOIET[ABETJOOTIS os NNW OD SN aua00g 91e7] tw omcosr ol N aus00q 91k] Qua00q 31e7 uolenteaa aaTelTUeNb eIO[J WoIeIp jo a8y saxo[dwiod WO RIP ITIsTIAIOeIeEYD ‘asnof sisuayvun *9 “YG snypipvs *9 *quahind “WA ‘UNID auahvd snosipour2s07 “s|ypey (uty ye ‘AdID) szusnz “9 ‘asnof v7Ipa *¢ ‘unIn) 22y9801q sixfidouvydaig “unin (e1vaf,Q) SnyDIpvs snosipo)vAyy *(SuIO} Jo dnox8) -zyy (ay) 27vI7NS DuISO]a WW “HA Cuniy) vypwwas pj,a1m0UunNIsy ‘unin, vpis -14f “dea snydsoufjod snpnviwapyy ‘unin, wnsasiav)9 (4) sosaz0javyD “IY Snyvipvs *9 ‘wuafiod “ieA ‘unIn 24ahnd 9 ‘unin snuod -0O49DUW “IBA 1491720 snosipoulIs0)7 *(sus0j Jo dnozs) syvey (uly 78 “A@ID) siuun? “¢ ‘unig 2y2801g sixidouvydazg ‘unin (e1ROW,O) SN7DIpvA snIsipo,vAYy *(SUIIO} Jo dno) *zyy (ayq) v7pI7Ns DiIsojayy "HA (unig) 270WwWads DpJaImounsH satoads Aeyo dyTTEztes8 ‘antag Ae OMIT -dZ1e8 ‘MOTIOL ASopouary 9Z-19VE T9VvE €—®O9VE ‘ou atduies (panutuod) og JIGVL 134 (126) =“ N —< uotjenyeAd dA TIeINUeNb “Masa(Q (Z[NYIS) sourW “GEA “Gq “LV ‘pypjnaidnig “itA “Sud (ulma]) v7v7nI2dn1q sisdojpnjiavy “WU | DIDISDY “AVA 7 *G “Z[NYIS soUurW *y VPVINIIdDY “IBA *] “CT “DYJUVIDIAT *{ DYJUVIVIAZ “IVA “AYA DYJUDIDIAL “GG “DIDPUNJOL “IVA BSNOL VIDpUN}OL * CT "Las -O[) DJ4990UI “J S2juarDI “AeA *f °G *$1]Ua.l -DI “| JaSID Sijuasva “IeA “ff °C yjanduass “IBA [JOM pJansuasf vy9I0hj21q ‘Jaseyy) (z[Nyos) sowrw “ana “g “VV ‘pypjnoidvig “1eA “Sualg (‘uluwia]) v7vj7nI1d01q sisdozno1avN WW] vjpjsvy “IRA “7 °G “Z[NYOS 4ourm “4 pyojnoidy "ABA DYJUDIvIAD = ‘DIVpuNnzvost “IBA BSROL DJ VpUNjOL‘* “las -8[D DJAAIUI “} Sijuasva “1eA “f °G *$1]UaIDI “J JOSI{D $17 -UddDD “IRA 1I7JANFUaIf DYVOli}IIG “LOSa[t) (Z[NYOS) sour “APRA “GQ “N “‘pipjpnjidvig “ARA “Buely (‘uIuIa Ty) Y7D7NIIdvIq_ SisdopnrIaDNN “4os -O[f) 4OUTW “} SIW4auI “seA “7 “GQ “WUT vypisvy “AeA “7 °G satoads soleppaseyooyrs aua00q 91°77 aud004 21k] aus00q 31v'] PIO[J WOIeIp jo asy uolleny{eAa At eITueNb TILA (unig) vjpwwes vjpa1mounsy ‘1ahivd 14ahvd = snosipourss0g *(suJ0J Jo dnox8) -zqy (1yq) D7IDIINS v«AISO]ap *SIUDUUIB PY JO sseul ‘e1O]J padrasaid AyIO0g “CRA CUNID ‘IY SnpMIipps “oD ‘qaafvd “aes ‘undy tsafind +9 ‘unsyy snsodos -IDUW "IVA 149]]20W SnaIsipoulIsoD “SIPPY (UY Ja “AdID) stung “9 ‘asnof vjIpe “¢ ‘undn 2yIso01g sixfiidounyday ‘undy (Q1ed|V,Q) snyvIpvs snosipo,vAyy *(SuIOJ Jo dnoi3) “zyy (ay) vyva)Ns D4sIS0ja pW ‘HA (UNID) DJoWwes v2}aIM0UNIn ‘unin vps jsf ‘des snydsowfjod snjpnviwayy satoads soxatdwiod wioieip otsta1deIRYD Aeyo ayt[azres ‘anyg £0S€ Aeyo ayTTezres ‘ant OLVE Kejo aytpaztes ‘anid | qZ-19Ve ‘ou ASojouary aqduies (panutiuods) og AIGVL 135 Vasyugan'e profile (from the collection eft: 1. Osyke, 1557) Well 3-k 61.0—119.05 m _ White, silty, slightly micaceous, poorly laminated clay with numerous plant remains underlain by varigrained and fine-grained, light gray and brownish gray sands. Chegan suite — Pg3— Pg} 119.05—165.95 m Green, silty clay with numerous pockets and "prisypki" of gray micaceous siltstone and fine-grained sand, as well as inclusions of oxidized pyrite and lignitized plant remains, underlain by interlayers of whitish gray, micaceous siltstone. 165.95—172.95 m Silty, brownish yellow, dense, unlaminated clay with plant remains. Yellowish green clay laminae in the lower part of the stratum. 172.95—193.9m_ Silty, light green, laminated clay with oxidized pyrite and fine-grained glauconite. 193.9 —201.9m _ Light greenish gray clay, more homogeneous than pre- ceding clays, with sparse accumulations of siltstone and pyrite inclusions, as well as pocketlike accumulations of glauconitic sand. Lyulimvor suite — Pg}~3 201.9 —210.4 m Clay, as above but more homogeneous, with numerous irregular, pocketlike accumulations of coarse quartz sand, also with rare worm trails. 210.4 —232.35 m_ Light yellowish gray and light gray, very homogeneous, clay laminae, irregularly gaizelike, with pyrite inclu- sions, pocketlike accumulations of fine sand and glauconite. 232.35 —239.85 m Whitish gray, gaizelike clay, in some places laminated, with "prisypki'' of micaceous siltstone on the planes of cleavage with numerous accumulations of glauconite; the clay is tripolilike in the lower part of the stratum. 239.85—267.45 m Gaizelike, light gray clay with interlayers of coarse glauconitic grayish green sandstone, dark gray siliceous clay and dark gray gaize. 267.45—274.45 m Gray (in places dark gray), gaizelike clay with an admixture of glauconite, quartz grains, isolated pyritized plant remains, small fish scales and worm trails. Underlain by rocks of the Gan'kino suite of the Maestrichtian. Four samples were examined from the core of well 3k; no. 1 (193.9 —201.9m, Chegan suite), no. 3 (232.35 —239.85 m, top), no. 4 (232.35 — 239.95 m, lower) and no. 6 (248.25 — 253.75 m); the latter 3 samples are from the Lyulimvor suite. 136 S S G € uoll -en[eAd ATIF -T1uUeNb (128) “1aSo]) VjL90U2 “J $17UaIDI “eA “f GQ 811 -uadvd *} Jasayy) s77uaivo “eA “f° “ayqjansuasf eA [Jad wpjansuasf *q ‘vingyf "J vpnqif “AeA “AYA vINGQI “pyajauiog “| sasal*) pjajdwoo ‘ied tadpuvpfap vyI0h}21q ‘unig, vjajdaiqns “IRA yo qaafvd “1eA “UNIS aiaiivd *9 ‘unin snuodosmvU “IBA 149]]20W * 2 ‘unig siupjod “ABA suassasvap *) ‘QsNOf SaplOUassaszap SNIS1poUIIs0) *(suuIO} Jo dnoi3) *zyy (‘ayy) 772097NS D41IS0]2 (raddn) G8°6Es —GECES aud004 a1e7] Zz ‘ g-vd ‘a2tns roAwtnk] Aeyo ayt[azteo ‘unpnaads “IRA ‘yoRH (Ay) Wnpnoads snuvydajsi(q “1asa[D (z[NYoS) 4owiw “AeA “q “A ‘pyvjnaidvig “IBA “AUdAT (wuway) v777nI1d01q sisdojn21av “DYJUDIDIA] “J DYyUvIDIA] “ABA “AY DYJUDIVIA] “CT ‘Tod vIs0nsuns, °C “Jasay (‘[Jaq) vsourds *q *1aSO]) JIaS “ABA “4 “GC ‘pIDPUNIOL “IVA ASNOL DIVpuNzoL “CT *1OSE]D V7L90UI “| S7qUauDI “IBA “f “GJ *$1]UaLDI “J Josef s1juaiv9 “AeA ayjanduasf *q ‘pyngif “yoingrf “wea “Ay vpNgQI{ “Gq ‘YyWlog ya “dway, 8729043 vppizhg ‘ID “VW s2q9vfjod snasipoursso) ‘rasa]) (¢) aua9 *(surs0j Jo dno3z8) pyonpoid *} Djajdwoo “AeA “Pp “q] -o8110 syvey (ury yo “AaIDH) stunz “9 *D}a] Ayreq ‘unin, Diodvdaw *¢ -dwoa *} 1asafy) 07a]dwoa “IeA *p “J ‘unig vypusuvm sixidounydaig “rasan [7 249908 *(SULIO} JO $84-%3q Aejo D]NUL0I1q “ABA 1a4apuD] {ap DYI0h}I21q aie] dnoi3)*zyy (“ayq) V7DIZNS VaIsojzapy | *a1tNs ueBoyD Aapis-Apues uon - Ad e1OTj = satoads . ase wo01eT ; . 3 ; im -nuenb pur a1ns ojoyly wi ‘yidaq jo asy I SOIPTLABETJOOTIS saxatdwod woierp dtstis1oRIeEYD -UWies (oyksQ “I*L JO UONSaTIOO ayi Woy) atyoud a,ueBndseA ‘ease qO IPPIW ‘A-€ [19” Woy sotduies Jo uoTIeUTWIeXa OIdoosoIOTUI Jo sITNsoy “LE ITAVL 137 (129) NN wo oO N INNO SIO oN uon -en[Teaad aATIB1 -tquenb “MOR (‘ayq) snaisanydsiway snzidouung “dasa[t) (z[NYIS) sourw “1eA “qQ “A *pjvjnaidvig “ABA “Bud (wutoy) 2707nI2dv1q sisdojnaiavAy “DYyyUvI -D14] “| DYJUDIVIAZ “AVA “ANY “7° “(UUO"] DIDISDY “ABA “7 “GQ “Z[NYIS 410Uu -1u “| DpDjNIIdD “AKA DYJUDIVIA] “GT ‘p]vpunjos “LEA OSNOL VJVpUN;OL “GJ “UOT Dpnaiavu “Gq *19SO[) Vj19IUI “| S7]UALVI “AVA “f “GQ *S1]UALDI “| JOSO[) $1]UALVI “ABA “f *G “ayjjansuas{ “AWA “[JOC] 27,aNTuUesf *q “ppngif “) pyngif “ABA “ANG PINGIL *G *pjajdwoo *{ AdSo[r) pjajdwoo “sed laspunjfap vyI0/}21q “Ov (ayg) snauapydsiway snjidouun) “L9Sa[ (Z[NYIS) sour “1eA “Q “NV *pypjna1dvn1q “ABA “BUILT (‘ututay]) 27n7nNI1d01q sisdoj)na1aDNy “DYJUDIVIA? “J DYJUDIVDIAZ “IRA “TYG VYZUVIDIAZ “GQ [JO Pisopsunsy “GQ “DIDPUNJOL “AVA YSNOL VJDpUNIOL *G sotoads SO1ET[ABETJOOTTIS aud004 a1e7] RIOT woe Ip jo o8y wh NOON ~t NN N o uoll -en[eAd aaTiel ‘unIg) 09249918 -]7S D411S0]9 “IRA DIDI JO SANTRA paiejos] "HA (UnId) DJDWwas D]JaIMOUNLy ‘IWog yo “duloy, s2729018 = vppIThg “ysnyqT (Qlop) v7dpnozra +7 “qlox] Djvavoxra vIaIvUIL | ‘undg) Djazdaugns “IBA “IeA tundy juafhvd “9 ‘unig snaod -O4IDU “IRA 140]]20W sndsipoul2se) ‘asnof vzpjIund “¢ ‘asno, DyIpa “gs "unin 22YIS804q sixhdouvydajy “und snasipo)vhi fT *(SuI0J Jo dnoi3) *z)y (ay) v7yvI7Ns vaIsOja py yea asafivd (Buea, O) $n]vIp DA ‘HA Cunin) vjvwwas vp]}a2N0UuNLyD ‘Wog yo “dway s1719049 = vppIxhig sotoads -TueNb saxeatduiod WOleTp ITIsTIBIOeIeYD Zz ‘ o- 28d aiins roaut{nky | ayllezte5 | —Sz' ghz z ‘ g- 38d aiins IOAUIT[NAT Keto aytlezteo (raddn) Keto |Gg°6ez— aytpTeztrey | —GE CES ase K3 ‘uid bse signe ojoyity =| w ‘yideq (panutiuos) Te a1dVL Zz ‘ gevbd ‘aatns roAwr{NkT 138 The first 3 samples contained diatom frustules and silicoflagellate skeletons, while the last sample contained only isolated valves of Melo- Sire sulcata var. siberica Grun. (Table 31). The diatom complex found at a depth of 232.35 — 239.85 m in the Lyulimvor suite is characterized by abundance of varieties of Melosira sulcata (Ehr.) Ktz. and the presence of considerable amounts of Grunowiella gemmata (Grun.) V.H., Coscinodiscus payeri Grun. var. payeri andvar. subrepleta Grun., and in the upper part of the zone also C. decrescenoides Jousé and C. decrescens var. polaris Grun. Limited numbers of frustules belonging to Pyxilla gracilis Temp. et Forti are also found. On the basis of these traits, the complex can be regarded as analogous to the Late Eocene complex of the Lyulimvor suite of the West Siberian plain and the Irbit suite of the eastern slope of the Urals. 130 The silicoflagellate complex of these samples consists of 14 species, varieties and forms. In both samples Dictyocha frenguellii var. carentis Gleser f. carentis, D. rotundata.Jousé var. rotundata, and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata are dominant. In addition, there are smaller quantities of Dictyocha deflandrei var. completa Gleser f. completasr D.cfibwula,Ehr. war. tipula,¢..fibula,.Di.irengiwellii. Dell. var. frenguel lis and Naviculopsis biapiculata var. minor (Schulz) Gleser, as well as individual skeletons of Cannopilus hemisphaericus (Enhr.) Hack. The lower sample differs from the upper one in the presence of very rare or rare skeletons of some varieties and forms of Dictyocha triacantha Ehr...and D. navicula Ehr., the lower density of D. frenguellii var. carentis f. incerta Gleser and higher density of varieties of Naviculopsis biapiculata (Lemm.) Freng., and also absence of skeletons of Dictyocha transitoria Defl. The sample from the Chegan suite (no. 1, 193.9—201.9 m) contains a diatom complex differing considerably from that found in the Lyulimvor suite (Table 31). Pyxilla gracilis Temp. et Forti, Melosira sulcata (Ehr.) Ktz. (group of forms), and the varieties of Stephano- pyxis turris (Grev. et Arn.) Ralfs are dominant. Among the species of Coscinodiscus, C. polyactis A.Cl. is encountered rarely, while the genus Stephanopyxis is characteristically represented by S. marginata Grun. andS. megapora Grun. This complex is analogous to the diatom complex of the lower parts of the Chegan suite or the upper horizons of the Lyulimvor suite of other areas of the West Siberian plain and the eastern slope of the Urals, and can be placed conditionally in the Late Eocene — Early Oligocene. The silicoflagellate flora consists of 14 species, varieties and forms. Among the dominant forms are 2 varieties of Dictyocha rotundata Jousé, D. deflandrei var. completa i. praducta Gleser,; -D. fibula Ehr. var. fibula f. fibula and Naviculopsis biapi- culata var. minor (Schulz) Gleser. Dictyocha frenguellii var. carentis Gleserf. carentis, D. transitoria Defl. and D. deflandrei var. completa Gleser f. completa are encountered frequently. The remaining forms are very rare or rare. 139 Parabel' area, Parabel'—Chuzik profile (from the collection of D. V. Osadchei, 1957) Well 7-k 5.95—101.55 m Sands, sandstones, siltstones. Chegan suite — Pg3— Pg} 101.55—147.25 m_ Silty, light green clay with thin "prisypki" of light gray micaceous-silty material underlain by interlayers of sand and sandstone. 147.25—153.25 m Clay — silty, greasy, light green, laminated clay with pocket and ''prisypki" of light gray sandy-silty material with pyrite grains and areoles of ferruginization. 153.25—175.85 m Light green, dense, laminated, silty clay, slightly gaizelike in places. Lyulimvor suite* — Pg373 175.85—214.85 m_ Silty, whitish gray clay with greenish tinge and with thin ''prisypki" of siltstone. The clay is unlaminated and easily soiled. The greenish tinge gradually decreases toward the bottom and the rock becomes more silty and easily soiled, sometimes diatomitelike. 214.85—228.25 m_ Light gray, argillaceous, dense, unlaminated gaize, with conchoidal fracture; fragments of dark gray, almost black silicated rock with conchoidal fracture are encountered. At the bottom of the stratum there are interlayers of silty diatomaceous clays gradually merging with gray, argillaceous gaize with conchoidal fracture. P F mt Gan'kino suite — Cry, 228.25 —281.45 m_ Light gray, silty, calcareous clay with pyrite pockets, worm trails, fragments of pelecypod shells and sparse plant detritus. Slavgorod suite — Cr,” *°P 281.45—319.35 m Silty, gray, micaceous, irregularly and slightly gaize- like, noncalcareous clay with pyrite grains, worm trails and sparse plant remains. 319.35—363.65 m Light gray, silty, gaizelike clay with pyrite grains and with conchoidal planes of fracture. This is underlain by oolithic ferruginous sandstone. * According to T. I. Osyko, the boundary between the Chegan and Lyulimvor suites passes higher, at a depth of 174.25 m. 140 G "$1]UILDI “| LASO[X) $17UILDI “ABA “f NG I ‘nyjansuaaf “AeA “[Jaq wpansuasf *q S ‘pyngif *y ving “aes “ayy DING’ “GC “Lose € pjonpoad ‘} vjajdwoo “IWA “Pp “GQ ‘pjayd fe -wio2 “| dasa, vjajdwos “IRA “p “Gq *19Sa[D J pjNUs0I1gQ “ABA taspudjfap vYI0h}21q ¢ “qosay (z[nyos) 4ourw “eA “Q *N ‘pyvjnaidnig “AkA “SUALT c (‘uruta’y) 77D) NI2d01q sisdo]na1av AJ *z[nyoS = 40Uu i Wl *} Dyvjnaidp “1eA vYZUDIDIA} °C ¢ ‘Tod Bo0psuvs] °C Yy *“lasa[) DjIas “IVA “4 “GC G ‘DIDpUNJOL “ABA “9SNOL DIVPUNZOL * (J y ‘JOSO[D Vj4aaUI “J $27UALDI “TBA eT "s1quadvo “| Vi JOSo[ S1qUaspa “ABA I2QJaNBUas{ “CT iG ‘pynqif "| vpngif “ABA “AUG ppnqif “qd “1asapy a pjonpoid *y¥ Djajdwoo “IeA “p “q *Dja) ¥ -dwioo *| dasajy vja7dwoa “lev "p *G *19Sa[D y pynusorig “IBA raupuDz{ap vYI0h}I1q uoll ay satoads aATIeI -tjuenb SOIET[ABETJOOTIS *(suti0j yo dno) sjey (uly 48 “AeID) sting “¢ ‘unin, viodvsaw “¢ ‘UnIH DIDUIZIDW *¢ ‘und 12YyI9801q sixfidouvydajg ‘unig snosi po) Dh yy *(suuJOj jo 21e] dnox8) ‘zy (‘ayq) 27DI7NS v4IS0]a WW D ieee (e1eveW,O) snzvipvs ‘yWog yo “dutay, s2y29n48 vypizhig 1D ‘W siqavfijod 9 ‘IYQ SNsLD snasipoUurIsoD ‘asnof apuzjaqvz “JB v4ISOISSY]DY | ‘(suizoj Jo dnoa8) = Sj[ey (‘Ury 19 “A@ID) S144n] sizfidounydajg Aqaeg eb? snasi po) vA yy -9uU9904 “(5tuI0} Jo a1e7] dnois) *zyy (AY) 27092NS D4Iso]a pW (2) aua9 -08110 (e1edfy,O) snyvipds uotl -en[ ead PIOTJ 1 satoods aanei Me dec muenb jo a3sy soxotdwiod WioIeIp ITAsTIBIOeIeEYD g- abd ‘o1ins IOAWITTNAT ‘Bafa ‘auins ueBeyD ase pure a1mns ASojoyi1 Z ¢c'091— —Gcest | JF ‘ou aid -wes (rayopesO “A JO vOOaTIOO eyI Woy) aTYoud HIZNYO-,Jaqeied ‘Pare qO PIPPIN “A-L Il9M Woy sojduies Jo UoTIeUTUIeXS SIdodsoIOTUI Jo sNseY “Ze ATAVL (132) 141 (133) = tN 5 SONS Ww Lic Veen ee! uot] -enyeAo ATE} -tuenb “eH (ayy) snaisapydsiway snjidouun) “L9SO[ (Z[MYOS) sowlW “1eA “Gq “NA ‘pyvjnI1dv1q “ABA “BUI y (ue) 97D7)NI21dn1q sisdojnI1av AJ ‘WW DIDISDY “IBA “7 "GQ ‘z[NYyoS «ou -1W "| DjD)NIIdD “ABA DYJUDIDIAZ “GT "1J9d visopsunsy *G ‘DJVpUNIOL “AKA ASHOL VJDpUNzIOL “J "1OSO[) VJLIIUI “| SIPUALDI “AA “f *G *S1]UALDI “J LASO[) $1]UaLVI “AURA “f “GJ ‘Ijansuasf “AWA “|Jac] AppJansuasf *q “‘Dyngif “sy DpNgif “ABA “ANS V7INGIL *G DID] a “ABA JISPQ VjJV]a vYyI0h}I21q “(ed ‘puotia “aa 7927d17)a Daa “MOST (ZjMYIS) sour “IRA “Q “NV ‘pyojnaidpig “ABA *HUdI (uud'}) v7n7nI1dv2q_ sisdojnjaDNy “Z[NYIS sou -1Uu "| DjD]nNIIdv “JeA DYUDIVIA *G [JOC PI4071sud4] “G7 "LOS9] VjIes “TWA “4 1G ‘DIVpUNIOL “IBA OSNOL VjJVpUNzOL * “LOSO[) Vj4aour “YF $1]UIIDI “IRA 117,aNsUaAL{ DYI0h}2q sotoeds SO] P[[IBe[JOOTIS 9ud904 a1e7] 3u2004 a1e7] NSFN OO 1O uot] -en[eAd PATIEI -tjuenb PIOYJ WO1e1p jo a8y “HA (undId) D7DW Was DIJaIMOUNID ‘Iloy 4a “dulay, s2q29p4d = j72.rAig ‘tuahod “1eA ‘unin tafivd *9 ‘OSNO[ Sapi0UuadsasIap sndsipoU1Izs0)D *(su10j jo dno13) sey (uly 4a “AdIN) stun? “¢ ‘osnoy vpipa sixfidouvydajg *(SUIIOJ JO dnoi3) *z)y (“4yq) V7VIZNS vAISO]a WY ‘HA (undiy) vjpwwas pjJa1m0UNLy ‘oq 4o “dulay, s1729048 vppIzhig ‘quahvd “leas ‘unig tahvd +9 "UNIN) suadsaizap “9 ‘asnOf SaploUudaIsasIap sg) ‘IUQ SNd1D snIsipou19s0D sotoads saxe[duiod woielp o1stIaIOeIeYD ei 84 ‘oqIns JOAWITINAT S896) — —G8'Gst € g-e3d ‘o1Ins JoAwt{nkT re “Ou ase AZojouqy] atd pue 93Ins -wies (penutuod) ze ATAVL 142 134 A total of 5 samples from the core of well 7-k were examined micro- scopically. Samples from the Chegan (no. 1, 153.25—160.25 m) and Lyulimvor suites (no. 2, 177.25—185.85 m; no. 3, 185.85—196.85 m) contain abundant algal remains. On the other hand, no algae were found in the samples of the Gan'kino (no. 4, 228.25 —238.95 m) and Slavgorod suites (no. 6, 319.35—329.95 m). Table 32 shows that the dominant complex of the deeper sample from the Lyulimvor suite includes species characteristic of the Late Eocene of other areas of the West Siberian plain and the eastern slope of the Urals, such as Coscinodiscus payer? Graon. var: payeri, C. decres- cenoides Jousé and Grunowiella gemmata (Grun.). In addition, the upper sample contains frustules of species of the Chegan suite, such as Coscinodiscus decrescens Grun., Stephanopyxis margi- nata Grun., and S. megapora Grun. Valves of Pyxilla gracilis Temp. et Forti are encountered more often here than in sample 3. In samples of the Chegan suite (or the upper part of the Lyulimvor suite, according to T.I. Osyko) valves of Melosira sulcata (Ehr.) Ktz. (group of forms), Stephanopyxis turris (Grey. et Arn.) Ralfs (group of forms) and Pyxilla gracilis Temp. et Forti. are dominant. Valves of characteristic Late Eocene species of Coscinodiscus and Stephanopyxis are absent; also absent are frustules of Grunowiella gemmata (Grun.) V.H. Frustules of Thalassiosira aff. zamelinae Jousé and Coscinodiscus polyactis A.Cl. are of frequent occur- rence. Because of these features, the complex can be placed tentatively in the Late Eocene — Early Oligocene (?), Core samples from the Chegan and Lyulimvor suites of well 7-k contain 17 silicoflagellate species, varieties and forms. Dictyocha frenguellii var. carentis Gleser f."carentis is dominant in the deeper sample, and abundant forms are D. frenguellii var. carentis f.incerta Gleser, D. rotundata Jousé var. rotundata and varieties of Naviculopsis biapiculata (Lemm.) Freng. The silicoflagellate complex of the upper sample of the Lyulimvor suite is more diverse and rich. Dominating here are Dictyocha frencuellni- var. Carent irs Glesericecarentis and ft. imeerta Gleser, D. rotundata Jousé var. rotundata, D. transitoria Defl., D. fibula Ehr. var. fibula f. fibula and varieties of Navi- culopsis biapiculata (Lemm.) Freng. In addition, this sample includes considerable amounts of varieties of Dictyocha deflandrei Freng. not found in the deeper sample. Thus, the complex of the Chegan suite is characterized here by an abundance of both varieties of D. rotundata Jousé and a greater con- centration of varieties of D. deflandrei Freng. Well 10-k 1150 — $8.3. m Silty clay, light gray with greenish tinge, with interlayers of sandstone and plant remains. 143 Chegan suite — Pg3— Pg} 88.3 —127.0 m Sandy-silty and silty, light green, micaceous, un- laminated clay with pockets of fine and medium-grained quartz sand and thin, whitish gray micaceous "'prisypki"' of silty material with pyrite and isolated plant remains underlain by slightly cemented, unlaminated, greenish gray, micaceous, fine-grained sandstone. 127.0—156.5 m Cemented, grayish brown, yellow-gray, dense and very solid clay with carbonized plant remains underlain from about 130.0 m by a medium-grained, unlaminated, slightly cemented yellowish gray sandstone with plant detritus. 156.5—173.15 m_ Silty clay, grayish white with greenish tinge, irregularly and slightly gaizelike, with small grains of pyrite, and in places with thin "prisypki'' of white, micaceous silty material; sparse pockets of fine, quartzy- glauconitic sand. Lyulimvor suite* — Pg}-3 173.15—186.25 m Silty, grayish yellow, micaceous, slightly gaizelike, dense, unlaminated clay with "prisypki'' of gray micaceous material in several places and interlayers of gravelly, unequigranular glauconitic sandstone with gravel, quartz pebbles and opaline cement. 186.25—206.55 m White and grayish white, gaizelike, silty, easily soiled, fairly light, sometimes diatomitelike clay; in places contains gravel-sand and quartz-glauconitic material. At the end of the interval there is an interlayer of dark gray silicified clay. 206.25 —221.15 m Dark gray with greenish tinge, silicified clay, irregu- larly mixed with quartzy-glauconitic sandy material, underlain by fine- and medium-grained, grayish yellow sandstone. At the end of the stratum the clay is silty, micaceous, irregularly gaizelike and light gray, strongly calcareous, micaceous and unlaminated with sparse plant detritus. Gan'kino suite — Cr;" 221.15—303.85 m Light gray and whitish gray, highly calcareous, irre- gularly gaizelike clay with sparse plant detritus, pyrite pockets and worm trails. * According to T.I. Osyko, the boundary between the Lyulimvor and Chegan suites passes higher, at a depth of about 156 m. 144 136 Slavgorod suite— Cr, °° 303.85 —345.10 m Silty clay, gray or gray with slight greenish or bluish tinge, irregularly strongly gaizelike with masses of sandy material, pyrite pockets and sparse plant detritus. Five core samples of well 10-k were examined. No algal traces were found in the sample from the Slavgorod suite (no. 12, 328.05—336.95 m) and 3 samples from the Gan'kino suite ine, Go 221.15—225515 m; no. 7, 225.15—231.15 m; no. 8, 231.15—241.15 m). On the other hand, sample 10 (155.5—162.7 m) from the Chegan suite contained abundant remains of a diatom and silicoflagellate flora (Table 33). The dominant diatoms of Pyxilla gracilis Temp. et Forti and Coscinodiscus polyactis A.Cl.; characteristically present are small amounts of valves of Stephanopyxis marginata Grun. and S. megapora Grun. This flora resembles the complex found in the lower part of the Chegan suite in well 3-k of the Vasyugan profile and well 7-k of the Parabel'-Chuzik profile, a complex placed tentatively in the Late Eocene — Early Oligocene. A total of 15 silicoflagellate species, varieties and forms were found. Most abundant are varieties of 3 species — Dictyocha deflandrei Freng., D. rotundata Jousé and Naviculopsis biapiculata (Lemm.) Freng., as well as Dictyocha frenguellii var. carentis Gleser f. carentis, D. transitoria Defl., D. fibula Ehr. var. fihula f. fibula. Well 15-k Lyulimvor suite — Pg}-3 170.0—186.9 m White, slightly micaceous, light, easily soiled diatom- ites with sparse laminae of siltstone overlaying silty, light gray (in places with slight greenish tinge) gaize- like, slightly micaceous clay, in places blending into light gray gaize. This clay is underlain by silicified dark gray, unlaminated clay and medium and coarse graded, green, argillaceous, glauconitic sandstones, in some places silicified with pockets of dark gray clay, pebbles and gravel. Gan'kino suite — Ge 221.55 —234.8 m Sandy-silty, gray, micaceous, irregularly calcareous clay with interlayers of sandy siltstone, with shell fragments and an interlayer of gray, micaceous, un- laminated, sandy limestone, dense in the lower part. 145 (135) == wo N wD st wom st NW stm uon -eny[eAo 2ATIEI -vquenb "19ST (Z[NYOS) s0W2W “IBA *q “NV ‘pyppnaidnig “1eA “Sued (‘uruIa']) 07D7nN21d02q sisdojna1aDNV "L9SO[) 10UIW “} S2W49aU2 “IBA “7 “G “UMA DzDISDY “IBA “2 “GQ ‘zjnyIg wou -1ul *} DjD]NIIdD “eA DYJUDIDIA. *G ‘Jad visopsunsy “Gq *1OSO]) VJIaS “IBA “4 “GQ ‘DIDPUN}OL “IEA BSNOL VJDPUNIOL * *19SO]D 07199U2 “| $27UaLDI “ABA “f *G ‘s1quaiDo *y JaSA]) $27UILDI “WA I1QJansuasf “Gq ‘Z|NYISG vUuosDJUad “IBA “{ “G ‘pyngif *y pyngaf “sea “ayy vpNGIf “GG *LaSe[D pjonpoid *j vjajdwod ‘1eA “p “Gq *D79] -dwoa *} Jasayo vjajdwoo “iRA ‘p *q *1asa[y DINUL0IIQ “JA 1adpuDj{ap DYI0h}2q sotoads S21P[[I@SeTJOOTIS PIOTJ wo1eIp jo o8y ‘IWog «*4e ‘duleay, s1729013 v2I7hig ‘ID ‘VW s8229nfj0d snosipoui9s09 ‘UNI, VIpawaajqu2 “IBA S1uunz *¢ ‘unin viodpsaw “¢ ‘UNI DIDUISLDW sixfidounydarg *(SuJoj Jo dnox8) *zyy (aq) 27D97Ns v4rs0]a Py uoll -enyTeaad ATIF -vuenb satoods Saxo[dwWiod WOIeIp OTIsTIsIDeIeYD ase pure aims ASojounT Ov ‘ou aid -Wwes (rayopeso “A‘d JO UOTIOBT[OO oY] WIOY) Bale qO STPPIW eyI Ur aTYoud YIzNYD-,[eqeieg ‘Y-OT [[9M Woy sotdwies Jo uoTIeUIWIEXS DIdOdsOIOTWI Jo si[NSOYyY “EE AIGVL 146 “MORH y (ayq) snoiuapydspway snjidouung "muIa"] snuos T -pjuad ‘eA wnjpnaads snuvydajsiq G “1ase[ (zZ[NyoS) sow2wm “TeA “q “N ‘pippnaidvig “ieA “sUaIy G (wulo}) vzvjnaidv1q sisdojna1a0 Ny € ‘HA (unin) 07DWwWad DIJaIM0UNIH “pyyuvav fe ‘yoy yo “duet, 2729018 vpjIxhig i 147 ‘J DYyJUDIVIA? “IRA “ANY “2 “°C € ‘qsnqT (qtoy) 27djnora vI49vUI4 J Z “{OSI]H LOUIW “| SJW4aU2 “IEA “7 “G ¥ ‘ds snosipoui9ss09 e “WIWa] DIDISDY “IVA “7 °C Ui ‘uahod “IeA “uNID 24afvd *9 *‘ZjNYISG s0U G ‘unIn snsodo1gDW “IRA 14911720 * 2 I -1Ul *} DID]NIIdD “IVA VDYJUVIVIAT °C € “IYW Snsuv snasipour9so) G ‘DJVpUNIOL “AKA OSNOL VIDPUNIOL “J Z ‘asnor vyvj2und «‘¢ “10S € ‘unIn Diodnsgaw “9 c -O[ Dj199U2 “J SiquasvI “IBA “f “G Z ‘unig 298019 sitfidounydajg 9 "$2]UALDI "| AVSO[D SI7UALDI “LEA *f ‘(TT “undy C ‘qyyjansuaaf “led “Jad 2pjansuasf “Gq G (e1eaJV,O) SnjIVIpV4 snasipojvA yy ses € “pingif “| vpnqif “dea “AY BINQI{ *q | 21990d *(suusoy Jo gered oun O'6LI 1 "DyVIa “ABA LOSI] VjvJa vYI0h}2Iq ae] G dnoi8) ‘zyy (AU) B2D2]NS Dsis0ja Wy joaurtnk | aitw0ie1q —0'0LI voll -enjeao uol -eny[eaad satoads RIOT} satoads ‘ou ae: W101e1 ek ae ASoyouit wi ‘yido aid -tluenb ” -luenb pue 211ns TeUa te 1 jo any ‘ -wes Sa1PT[ASeTJOOI[IS SdXd[dUIOD WOIkIp ITISTIBIOPIeYD Il poor! I pot (rayopesO “A “d JO UOTI2T[ON 941 WO) GO eTPPIW 24) UI at youd yIZNYyD-,[eqeied *Y-SGT [[oM WoO sojdwies Jo uolleUuTWIeXxa odtdoososstw jo synsoy “PE ATAVL (137) 147 Slavgorod suite — a 395.6 —414.0 m Silty, light gray with slight greenish tinge, somewhat gaizelike clay with pyrite grains and worm trails. Sandstones of the Kuznetsov suite of the Turonian begin at the end of the interval. Two core samples of well 15-k were examined. No trace of algae was found in sample no. 5 (395.6 — 403.6 m) from the Slavgorod suite. On the other hand, there were abundant algal remains in sample no. 1 (170.0— 179.0 m) from the Lyulimvor suite (Table 34). Among the abundant forms are Melosira sulcata (Ehr.) Ktz. (group of forms), Hyalodiscus radiatus (O'Meara) Grun., Coscinodiscus payeri Grun. var. payeri, and Coscinodiscus sp.; frustules of C. argus Enhr., Stephanopyxis megapora Grun., Trinacria exculpta (Heib.) Hust., Grunowiella gemmata (Grun.) V.H. are frequent, and there are also small amounts of Stephanopyxis broschii Grun., S. punctata Jouse, Coscinodiscus moelleri var. macroporus Grun. and Pyxilla gracilis Temp. et Forti. These species are characteristic of the Late Eocene flora of the West Siberian plain and the eastern slope of the Urals. A total of 14 silicoflagellate species, varieties and forms were deter- mined in this sample. Dictyocha frenguellii Defl. (group of forms), D. rotundata Jousé var. rotundata and varieties of Naviculopsis biapiculata (Lemm.) Freng. are dominant. Among very rare forms are Distephanus speculum var. pentagonus Lemm. and Cannopilus hemisphaericus (Ehr.) Hack. Thus, the material obtained from well bores and natural outcrops in many parts of the eastern slope of the Urals and the West Siberian plain consists of silicoflagellate complexes belonging to the Upper Cretaceous, Early Paleocene, Early, Middle (?) and Late Eocene, Late Eocene — Early Oligocene (?) and Early Oligocene (7). CENTRAL ASIA, ARAL-CASPIAN AREA The silicoflagellate content of rocks of the Tas- Aran and Saksaul'skaya suites in the Turgai Gates was examined. The Tas-Aran suite has a wide distribution in these areas. It is divided into 2 subsuites: the lower, Tyk- 138 Butak, composed of sands, sandstones and clays, and the upper, Ak-Chat, consisting of bluish gray clays, gaizes and gaizelike clays (''Resheniya Mezhduvedomstvennogo Soveshchaniya. . ., 1959). Both subsuites are characterized by a marine fauna of mollusks, foraminifers and radiolarians. Yanshin (1953) places the Tas- Aran suite in the Middle Eocene and the lower half of the Late Eocene; Boitsova et al. (1955) place the suite in the Middle Eocene. On the basis of the foraminifer and radiolarian fauna, Lipman (1960) places the age of this suite in the Middle Eocene and partially the Late Eocene. According to Ovechkin (1962) the lower Tas- Aran subsuite (i.e., the Tyk-Butak suite) belongs to the Middle Eocene, and the upper Tas-Aran subsuite (Ak-Chat suite) to the lower half of the Late Eocene. 148 (139) N= = Sone) uoll -eny{eAa SATIEI -T1uenb AOTTEUAT ‘Wg JO SuoTIDaTTOO ay2 Woy) (aATY z1Z3q ayi jo Arein *p]D1Nd -idp "J “WiWaT pjpjnaidv “1eA “4 °C 10se[9 -peiys) vsonzaj{ “1eA DY;UDI (190 D147 °C ‘rase[) (‘[Jad) vsourds -q “Z[NYOS VIIQuoys “J ppngif “1eA “f° mL “Wed Ris ot pingyf ‘AeA “AYA vjynqif vys0h771q (zjnyosS) vyD]nIIdv “jye YUII0Sa *1989[D (‘dAe]-"Id) Sapi0j1douuvs “1B “mwa snuospjuad “1eA wnjNn ‘Enda ‘yoeH (ag) | Tn49 ‘JasepH (zjnyos) sowiw “IBA Acs @ gads *q "TeA snupydajsiq "9 °N “Jase[) (Z[NYOS) 0792478 -uod ‘1eA vyvjn2idv1q sisdo] nI10D AY “UIWIOT DIDISDY “IRA “7 "CT “pyD] NI -idp *y ‘wway vjnjnIIdv “Ie 1ase[) Aad (rat -peiys) vsonrayf “eA DYJUDIVIAT °C ‘raso[y) (‘[Jaq) vsourds “gq “‘Z[NYOS vYyJUvIDLaY *(T “MIUe'T (“yORH) snquoys “vA pyngif “yye -d ‘mngyt °§ pingyf ‘aeA “ayy VpNgQrf vYy20h}21q satoads SI1IL[[IABETJOOTIS auso00g 21°] 2us904 3187 PIOTI woe Ip jo a8V LOOM NWM ae Ot MID WD Ww 19 oO =D ST uw OD LD A OD OD SH uo -enjead dATIe1 -tuenb ‘unig (‘Iyq) vuos09 sixidouvydazs yo eaAoussog 21129 v4isopodopnasq "uNIN, 09219918 AG. Te! ‘unig $2704 nqI9}1YIAD D4L1S0]9 WY ‘unIg suDj1q7N4 010]F0;SD WY ‘unin 21y92A0p1a “ye DINIIAD Ny ‘gsnor simuaj ‘deA DIIUavI05110 “dq ‘og 4@ ‘due, s2729043 ppt ‘radoy (“[ted) -0au “JPA Wnt ‘Ss cy snipamsaqut ‘ds snasipo0ja1jsopnas q ‘unig vasogsadhy 011974914 “AYA ‘Iyq vs0qgozs sixfidoryjuvy *(susoj yo dnoi8) =Sj[PY (‘ury 19 °AQID) szuinz sizAdouvydaig 4a eBAOUSSOg 271299 v4ISopodopnas q ‘unIn §093.12q18 “ASE toe ‘UNIG $17D4Nj9ENYILD D.L1S0]3 WY satoads saxatdwiod woleIp STIsTI9IOPIeYD *1ase[ ‘IRA DIDIINS * IN sysuansvwvo * Wy "S ‘Vv visno{ “W Zz . o-38d ems ‘ds vuoydwy ahawony viydinppig “AGI, WNiDULOLA * J ‘unig, sisuapoad ovapuod WNI}7D12914 J snyahijdou1j9 py sngip sngasipou19s09 PCI) 69) “IRA DIDIINS *W IN) sisuanuvupo * 'S “VW Disnof *W z ‘ go g8d ‘ams a3e pue o11ns uely-seL uely-se Lb ASoyouarT 96 ‘ou ojdues (eaojdeaL *S “1 pur qin) raaty Aiyeney-,uezp oui Woy sotduies Jo UoTPUTUIEXa oidoosoi91w Jo sijnsay “Ge ATAVL 149 (140) =—N = Aa Sel oe | lop) st uo -enTeAd dAe1 -T1uenb ‘9d (zj[nyds) vjDjnNIdo “TTR DUaI0Sa yy “UOT snuosvjuad “1eA wnjnaads *q ‘EN42 “IA (ayq) @ns2 snuvydajsiq “lasayy) (zjnyos) 4s0U -1 "JeA DID]NIIdDIQ sisdojnj1av Ny “WUa] DIDIsDY “IRA “7 “GQ *pyv) NI -1dD "} *WIWa] DzDjNIIdD “IRA “7 “G “Lasa]s) (loup -B1}S) vsonraj{ “AeA DYZUDIDIA, “Gq [Jad Disopsunsy “G "4asayy (“[Jaq) vsourds *q ‘DIDpUNjJOL “ABA BSNOL DJVpUNjOL * “‘pingif *y “yy Dpnqrf vyI20hj21q “OVH pjynqi{ “eA “UWaT wnjnoads = "q *EN1I “IBA (ayq) wnsa snuvydajsig “Jasayy (zjmyos) «ou -1W “IRA DIDINIIdDIQ sisdojnjavN “WUIa'T DIDISDY “IVA "7 “GG DYyJUvI -D14] “JY vyqUBIVIA] “IBA *IU 7 OG snuospjuad "AeA “eH satoads SILT [AS eTJOOTTIS aud004 21e7 € G ¢ G i G G J J ¥ € 5 G y ¢ 5 y S 9 aua00q aie] uoTl -en[eAd aAT1e1 -tuenb PIOTI woieIp jo asy “V1T] UL BAOUSSOg DIvAANI “| DW17719D49 “IBA *3 “qd ‘WIT UL BAOUSSOg DwW12]19D45 “| pwijj19vis «= ABA 682719049 = DJ AThg ‘sedoy (‘[teg) thawon; viydinppig ‘uNIn, sisuapoud -0au “IRA WN4L0IE=PU0I WNI40D19914 J ‘(sluowSe yy) "S "YW Snipawmsajqur. snyrfzdourjap “YQ Sngip snosipouiss0g *(suii0j Jo dno) syjey (uly joa “AeIDn) siuinz? “¢ ‘unIg, (Yq) Duos09 sixidouvydayg *19S9]D ya eAOUSSOg 0712q Dulsopodopnasg ‘UNIN) DIILAQIS “IRA DzJDIINS “Pp 4S 48 “AD sisuanivuvo * py ‘UNIG $1704N}9971YIID D1IS0]9 WY ‘UNIDN 2y91A0p1a “Te “Ay $18U9I]1SD1Q “JIB DINIAVAT ‘UNIG SUv]17N4 D10730)]sD W ‘asnof simuaz “IBA DI1UaDI081]0 *q ‘Iwog joa ‘dway, s2719048 vp xhig ‘radoy (‘[teg) tfawon, viydjnppig “AOIT) WNIDULOLA * 7 ‘unIn) sisuappss -09u “IBA WNLOIAPUOI WNI]D19914 J ‘S "VW snipewmsaqur snyrhjdou19p “Iq vsoqojs sixhdoiyjuvy ‘unin, Dasoquadhy viyjam7yYs14g “IYQ Snsip sndsipouirs07 *(Suroj yo dnox3) syjey (uly 4a “AeID) siuing “¢ ‘unIy satoads saxaTduiod WOIeIp ITIsTIBIOeIeYD _38q ‘aims uely-se L 980) 334 ‘a1ins uely -Se L 96 ase ‘ou ajduies pue o1ins ABojoytT (panutiuos) se ATaVL 150 The overlying Saksaul'skaya suite consists of glauconite-quartz sand- stones, gray-green clays and siltstones. Yanshin (1953) places this suite in the upper half of the Late Eocene. Boitsova et al. (1955) note, on the other hand, that the molluskan fauna of the Saksaul'skaya suite is of a mixed nature and includes Middle Eocene as well as Late Eocene species. On these grounds, sediments of the Saksaul'skaya suite should be associated with the lower part of the Late Eocene. A series of samples from the Saksaul'skaya suite, obtained in a stratographic profile on the Manaul'e mountain, as well as from a profile of the Tas-Aran suite on Tas- Aran mountain, and cores of wells no. 1 (Turgai settlement), no. 62 (Tumalykol' settlement), no. 64 ( Chagrai plateau), no. 45 (town of Chelkar) and no. 46 (Lake Tebez) were examined. All these materials were obtained through the courtesy of R. Kh. Lipman and I. A. Khokhlova. Samples from the collection of B. M. Mikhailov and L.S. Teplova of the Tas- Aran suite of the basin of the Irgiz River onthe right bank of the Uzen'-Kairakty River were also examined. Most of the samples contained poorly preserved diatom remains and no trace of silicoflagellates. Rich remains of diatoms and silicoflagellates were found only in the Tas-Aran suite of the right bank of the Uzen'-Kairakty; these fossils were abundant but poorly preserved in rocks of the same suite near the settlement of Tumalykol'. Right bank of the Uzen'-Kairakty River, a right tributary of the*Irgiz River The outcrop lies on the right bank of the Uzen'-Kairakty, approximately 10 km from Mialy settlement. Thin, light brownish gray clays, in places light greenish gray, emerge on the surface and reach a maximal thickness of about 20 m; these are underlain by Paleozoic rocks. Two samples of these clays from the collection of B. M. Mikhailov (nos. 87 and 96) and one sample (no. 1086) from the collection of L.S. Teplova were examined (Table 35). Both samples from Mikhailov's collection contained a very abundant and well preserved algal flora with an almost identical species composition. Many of the species (Melosira architecturalis Brun, M.oama- ruensis Gr.etSt., M.fausta A.S., Actinoptychus intermedius A.S., ete.) are known as characteristic forms of the Kharkov (?) suite of the Ukrainian SSR; a large number of forms are widespread in the Late Eocene and Early Oligocene (?) deposits of Western Siberia (Tricera- tium exornatum Grev., Pyxilla gracilis, Temp. et Forti, P. oligocaenica var. tenuis Jousé, etc.). There are a considerable number of diatoms of the order Pennales (Navicula aff. vidovichi Grun., Mastogloia rutilans Brun, etc.) and new species form a large proportion of the flora. 141 A quantitatively poorer complex of similar composition was encountered in the collection of L.S. Teplova (sample 1086). A great similarity exists between the diatom complex of the Uzen'- Kairakty and that of the Kharkov (?) suite of the left bank of the Dnieper near Dnepropetrovsk. However, the former complex differs in the ' presence of considerable amounts of several species of Pyxilla. 151 R. Kh. Lipman, who determined the radiolarians of Teplova's collection (Cenosphaera sp., Spongodiscus sp.sp., Cenodiscus sp., Spongosteriscus sp., Lithatroetus sp., Serhocyrtis tamdi- cusis Limp., S. elegans Lipm., Serhocyrtis sp.), places the Uzen'-Kairakty clays in the Late Eocene. Their position in the strati- graphic section (Tas- Aran suite) is evidence of their Eocene age. The silicoflagellate complex of the Uzen'-Kairakty is very rich. The dominant forms in sample 87 are Distephanus crux (Ehr.) Hack. var. crux and Dictyocha aff. fibula var. rhombus (Hack.) Lemm., while D. triatatitha var: ‘apiculata ft aptculata ‘Lemms, Dit. var: flexuosa (Stradner) Gleser, and Distephanus speculum var. pentagonus Lemm. are rare; remaining forms are very rare. The silicoflagellate complex of sample 96 consists of the same species but occurring as isolated (very rare) specimens, except for Distephanus speculum var. pentagonus Lemm. which is rare. An analogous complex was found in sample 1086 of Teplova's collection (Table 35). In addition to the dominant forms of sample 87, Dictyocha spinosa Defl. is abundant here. D. triacantha var. apiculata Lemm. f. apiculata and Naviculopsis biapiculata var. minor (Schulz) Gleser are encountered in slightly greater numbers, as well as isolated specimens of Dictyocha transitoria Defl. and D. rotundata Jousé var. rotundata. Tumalykol' mountain Well 62, Tumalykol' settlement (from the collection of R.Kh. Lipman and I. A. Khokhlova)* Tas-Aran suite (upper part) — Pg33 20.00—77.65 m_ Light green, slightly sandy, dense, gaizelike clays with conchoidal fracture having interlayers of quartzy- glauconitic, micaceous and quartzy, densely laminated sandstones in the lower part of the interval. 77.65—115.45 m Dense, light green, dark gray, gaizelike, slightly sandy clays; light greenish gaizes with conchoidal fracture, laminae of green and dark gray clays, also with fine- grained dark green sandstone mixed with glauconite and a quartzy-micaceous material. In places fish scales are encountered. Four samples from this well were examined. No trace of algae was found in the lowermost sample (no. 23, 151.4 m). The remaining 3 samples, (no. 14, 91.6 m; no. 10, 67.7 m; no. 7, 60.0—66.15 m) contained a poorly preserved diatom flora as well as a characteristic complex of silicoflagel- lates (Table 36). The fossils were most abundant in the uppermost sample. * A description of the section of well 62 together with a detailed paleontological discussion can be found in the work of N. K. Ovechkin (1962). 152 142 “T° i ‘pueula “sy = 7927d1779 + DvuUav0sa Wy b ‘Jasoy snnbijuv snuvydajsiqg ‘pjpjnaidviq “JeA “BUeIA (‘uulay) vyvjnI2dv1q sisdopnnavyy i J *‘TJOqQ VI40jIsudvs, “GG J “JOSO[D 9902S “IBA DJVpUNOL “CG ‘DIpawu *{ J J9Sa[) VIpaw “JRA DIDIA py20h}21q ‘9d if ‘puoulo “IYO v214d1]]@ + oDUuar0sa py "Jaso[y (zjnyos) sou } -m ‘IeA vjv)nNI1dD1q sisdojnI1aAv NJ Z ‘Jase[ sunbiqup snuvydajsiq ‘zjnyog 10u | ~1UW *} SIWsau1 “IeA DYJUDIVIAZ “CT | ‘gasopy (‘[Joq) vsourds -q I ‘DIDpUuNjOL “IEA 9SNOL VIDPUNIOL °C Z “Saf VJINpas “| VIPaU “IBA ‘2 *G ‘DIpau “fy J Jasa[y) Dipaw “ieA vjvj]a vYI0h}21q “TJ9d J ‘puowia “IY 091701772 Duas0sa yy *1asa]y) (z[NyoS) sow i 1 “IRA DzID]NIIdDIq sisdoj,nz1av Ay y Jaso[y) snnbiyjuv snuvydajsiq zjnyog + 40U J -1u "| DyDjnIIdD “IBA DYIUDIDIAZ °C Z "19S9[Q DIAS “IRA “4 “GQ € ‘DJDpUNIOL “ABA ASNOL VJVpUN}OL *G 9 “19S9] VIINPas “| VIpau “ABA “9 "GT DIpau *{ c Jase] Vipaw “ies vjv]a vYI0/h}I21q uoll -eny[eAd a sotoads -1quenb SOIVT[ISETYJOOTTIS aua004 21k] aua904 e7] 39004 aie] PIOTJ wo1e Ip jo any -eny{ead ‘sluousey — (9snof sinuaz “IRA p21UavINSI7O “{9 ‘NIIUaDI08170 "IBA gsnof vI1UanI08210 “JO ‘1y10q 4a ‘dulay, s2jjapud =*'y9) 4 ‘ds njp1zhig *(sluowiSe yy) ‘unIn) vaL0guadhy v12)aNq 4514 F ‘UNID) SUaISaLIap sSnIsipou1IseD “1aseyH 4a eAOUSSOg 02]2q Dii1sopodopnas gq ‘ds sirfidouvydajg ‘unin viodvsaw sixhdouvydajg ‘(snoyiquin) ‘ds snosipojpAy ‘UND 0I149G1S ‘IBA DJDI]NS D41180]3 JY ‘squouseyy — (asnor sinuaz ‘IWA DIIUaDI0SII0 *JO) “ds vIpITig ‘(SqUaUIBeIy) Jase, yo BAOUSSOg 27]2q vuAIsopodopnasd ‘(snotjiquin) ‘ds snosipojpAy ‘UNI®) 09249918 ‘IRA DIDIINS D1180]3 WY ‘slususey — (asnor sjnuaz ‘J®A 4a =991UaDI0F170 “IBA 9SNOL VIIUIDI0TI]0 “JO ‘10K ya ‘dutay, saqiapad *yo) “ds vpjixhig ‘unin vasoquadhy vipqjanqysii g ‘(juow8ey) ‘ds vuajsopodopnasgq ‘(uoWwBey) JasatD yo eAOUSSOg 02]2q vsisopodopnasg ‘(snotjiquin) ‘ds snos2pojvhi yy *(SuIIO} Jo dno18) *zyy (‘aq q) 07VI]NS D«IsOja py uon satoods aaTei -vquenb SaxaTduod WOIeIpP ITIsTIDIOPIeYD ‘TAOSeqeya snyd -1xosdi{tg JO dUu0Z "9Ud909 91°T Zz ‘ god ‘arins UvIV-stL Keo va ‘TAOSeqeyo snyd -1xosdiqta Jo QUu0Z *QUd00g 21e7T peti ‘auins ueIy-se L KeID OF ‘TAOSeqeyo snyd -1xosdittd jo au0Z *QUua00q 21e7 ¢-¢3d ‘o1ms uvIY-Se L KeID ase a wi ‘yidaq| aed -WIes ASopouatT (eAoTyyoUM *V "I pue uewidry] “yy “Y Jo uotseT]oo oy) wo) wewetNes ,joyATeUMNL ‘Z9 1[2M WOY sotdures jo stskteur DIdooso1OTW Jo synsay “9G AIGVL 153 143 The bulk of the diatom population consists of fragments of several species of Pyxilla, Melosira sulcata (Ehr.) Ktz. (group of forms), Pseudopodosira bella Possnova et Gleser and Pseudopodosira sp. There are large amounts of well preserved silicoflagellate skeletons of Dictyocha elata var. media Gleserf. media andf. reducta Gleser and Distephanus antiquus Gleser. Dictyocha rotundata Jousé var. rotundata is frequent, while var. secta Gleser of the same species is rare. There are very rare specimens of a form belonging to Naviculopsis Freng. and another of Mesocena Ehr. emend. Defl. The numbers of silicoflagellates in the other 2 samples are poorer. FAR EAST Kamchatka Silicoflagellates were sought in the marine Neogene deposits of western Kamchatka (Kavran series) and eastern Kamchatka (Tyushevka series, the Blue Clays suite, the Sand-Clay suite, etc.). The marine deposits of the northwest coast of Kamchatka in the Rekinniki Inlet have been placed in the Kavran suite. The fine-grained rocks of light color and gaizelike structure belong to the upper Kavran subsuite (Kochet- kova and Khaikina, 1958). According to these authors the molluskan complex (Pecten, Pododesmus, Psephaea, Neptunea) resembles the fauna of the Etolon suite of the Kavran bed of the Tigil' area; they con- sequently place the upper Kavran subsuite in the Middle Pliocene. In the Tigil' area, the Kavran series can be divided into 3 suites. The lowermost suite is of a conglomerate nature and contains remains of a rich Late Miocene molluskan fauna. The conglomerate suite is continuously overlain by the Kakertok suite, which consists of fine-grained sandstones, diatomites and gaizes. Krishtofovich (1959) writes that the Kakertok suite was placed in the Lower Pliocene because of its stratigraphic position and the presence of species common to the overlying Etolon suite of the Middle Pliocene. Lithologically and paleontologically, the Kakertok suite is closest to the Kurasi suite and the lower part of the Maruyamu suite of southern Sakhalin, which belong to the Okokykai stage of the Late Miocene, and corresponds to the Oiwaka series of the Pliocene of Hokkaido. In Kamchatka, the boundary between the Miocene and Pliocene has been placed tentatively within the Kakertok suite. On the east coast of Kamchatka, the rocks of the Tyushevka series occur in the area of the isthmus of the Kronoki peninsula and near Ust'-Kamchatsk. The rocks of this series consist mainly of sandstones, argillites and diatomites. Gryaznov (1959) distinguishes between the 3 following suites. The lower — Ol'ga — suite consists of argillites, siltstones and diatomites; judging from the molluskan fauna, it belongs to the Early — Middle Miocene. The middle — Talovaya — suite is composed of interbedded sandstones, argillites and diatomites; it belongs to the Middle Miocene. The upper — Rakitin — suite consists of conglomerates, tuffs and sandstones with shells; according to the fauna, it is placed in the Late Miocene— Early Pliocene. 144 154 Samples were examined from the basin of the Bukhtovaya River, the east coast of the Penzhina Inlet, the Kavran series, the Rekinniki Inlet area (from the collection of A. D. Kochetkova, 1954), the Kakertok suite, Napana River in the Tigil' area (from the collection of L. V. Krishtofovich, 1957), the Tyushevka series of the Opala and Savana rivers (from the collection of V. L. Vdovenko, 1957), the argillaceous slates of the Miocene of the Volch'ya and Valunnaya rivers (from the collection of L. P.Gryaznov, 1952), the Tyushevka series rocks of the Ol'ga River (from the collection of V.N. Sarsadskikh, 1954), and from Neogene rocks of the Ust'-Kamchatsk area (from the collection of A.I. Yudin, 1953). Silicoflagellates were absent from most of the samples. TABLE 37. Results of microscopic examination of samples from Neogene deposits of Kamchatka Tyushevka series Napana Savana River, River area, Rekinniki Inlet, Kakertok ; Volch'ya F i basin : Etolon suite suite f collec- River Species (from collection (from ( 2 tion of (from of Kochetkova) collection - i Yudin) collec- ’ tion of P of Krish- tion of tofovich) Dictyocha fibula Ehr. var. fi- brela, Ss fibula:t sees oe eee D. {. var. pentagona Schulz Distephanus cruz (Ehr.) Hiick. D. octonarius var. polyactis (lore:)Gieser 22° Ors D. speculum (Ehr.) Hack. Wale SPECULUM. oe ats. cues, * D. s. var. pentagonus Lemm. D. s. var. septenarius (Ehr.) DOUG tee Mh het Upceh hel Z 1 4 oa — —_— — e —_— — — — — eS — = =a S + a 3 1 = J = 1 J ea Z = = z a on - * y J € 1 z z | S | 5 e —_— — —_— J — — — —— — —- — g oo = 1 b 1 } z i “3 = — —_— — — if — — ae — — — = ¥ = = + g J J = = € = € Y z — = $ = = 1 = _— — —_ if _— — — if — —_— — $ = 2 Z - = g y Z ¢ i 8LI “ou NOW fo uondaTfoo (yoTAOJo1Yysy jo uondeTToo) e[nsutuad apruys JO ySeOO UIOIsey UOTIDIT [OO JU TIDaTJOO) ieBsTyoRW| sida aye] pue | 18u07 pue JOATY Buoy unadoiy SIQATI TWIN] pue [suoy jo urseg NOW fo uotldeT[oo ADIJOIY JO UOTI9TIOO e[nsutued iprwiys uITeYyyAeS UIoyIOU JO J1INS WIIG G41 WOY satduies Jo UOTIeUTWIeXa DIdoOodsOIOIW Jo sNSaY “OF ATAVL (151) “"yoeH 070/378 vuar0sa py ee papiouazosau “y “d “dg * s1j90h} -od * ined ten DYyI0hjI1pvsvg ‘Blog (Iq) Snisvuajdas “ied “s “qv ‘WIulaT snuodpjuad “IBA ‘Ss “CT * asap (aAeq-Jd) sapiojidouups “IRA *s "qv -ads “eA “yoeH (Yq) wnypnoads *q -0190 “JA “[Jaq (Aug) sm14DU0}I0 "GJ fe ge ai oct. TG * wnjno * snilpu snI1Uu soda 4 vest) cp@) snaiuodvl -q IEA *YORTT eon nia snuvydajs) (7 Dinqi| “TEA rnd * Z]NYIS vuoFDjuad “TEA “f° ae DI1q Woy. a “wea “f° - pynqif | ‘SYa yng { vYyv0h}01q sotoads 162 Samples 148, 477 and 180 apparently correspond to the upper part of the Diatom suite of the Machigar section. This material contains a roughly equal amount of Dictyocha fibula Ehr. var. fibula f. fibula and Distephanus speculum (Ehr.) Hack. var. speculum. However, the density of silicoflagellates is greater in samples 148 and 180. Basin of theTroptun‘and*Loengi miver's A characteristic silicoflagellate flora was encountered in one sample (no. 509, collected by Erofeev) from this area. Distephanus japoni- cus f. pseudofibula (Schulz) Gleser dominates here; two other forms — D. japonicus (Defl.) Gleser f. japonicus and D. speculum (Enhr.) Hack. var. speculum — appear in negligible amounts (Table 40). Sample 178 (diatom collection of MGU) from an unknown locality inthe Shmidt peninsula contains a similar silicoflagellate flora which also includes isolated skeletons of Paradictyocha polyactis Freng. f. polyactis and Distephanus speculum var. cannopiloides (Pr.-Lavr.) Gleser. Basin of the Kongi River and Lake Machigar The silicoflagellate flora was examined in preparation 182 of the dried collection of MGU. Distephanus speculum var. septenarius (Ehr.) Jorg. is the dominant form (frequent); the remaining silicoflagellates are encountered in negligible numbers (Table 40). 152 Rastern coast of the’ Shmidt peninsula Only 3 silicoflagellate forms were determined in 2 samples (nos. 236 and 238) from the collection of L. V. Krishtofovich (Table 40). The skeletons of Distephanus speculum var. cannopiloides (Pr.-Lavr.) Gleser are distinguished by their large size and the presence of supporting spines. The silicoflagellate complex of the east coast corresponds to that found in the upper part of the Diatom suite of the Machigar section (sample 101). Western coast of the Shmidt peninsula, south of the mouth of the Pil' River (from the collection of N. B.Vassoevich) Mayam-Raf suite Bed 92. Silty, light gray clays with rare and very small sandy-silty lenticles and a very sparse pebble. Imprints of small pelecypods. Diatoms are present. 163 Bed 93. Thickness 5.5m. A horizon of carbonate concretions. Bed 94. A gap of 11.5 m. Bed 95. Strongly argillaceous sandstones with sparse imprints of _pelecypods passing into sandy clays with greater numbers of diatom (153) frustules; pebbles encountered. Thickness 37 m. Bed 96. Sandy-silty clays with small separate sandy-silty lenticles. Thickness 15 m. Bed 97. Similar gray clays, with diatom frustules, radiolarian skeletons, less frequently sponge spicules. Thickness 25 m. Bed 98. The rocks appear to be argillaceous diatomites (light, slightly sticky to the tongue). In the fault scarp, the light-colored rocks become somewhat darker downward. Thickness 37 m. Bed 99. Sandy-silty clays, occasionally less sandy and lighter, contain- ing diatom frustules, sparse, small, sandy-silty lenticles and pebble. Thickness 41 m. Bed 100. Two strata of sandstone with intervening clay member. Thickness 1.5 m. Bed 101. Calcareous sandstone of concretionary type. Thickness 0.5 m. Bed 102. Silty clays with small, irregularly shaped sandy-silty lenticles. The clays contain rich diatom deposits. Thickness 42 m. Bed 103. Silty clays with diatom frustules. In the outcrop, the bed is moist and consequently darker. Thickness 0.1 m. Bed 104. Sandy-silty, unlaminated clay, with plant detritus and diatom remains. Thickness 0.5 m. Bed 105. Silty clays with diatom frustules and sparse pelecypod shells. Thickness 19 m. Silicoflagellates were determined in 6 samples from this profile: no. 98, bed 92; no. 99, bed 96; no. 100, bed 99, and samples 105, 110 and 115 (collection of O.S. Korotkevich, 1958) (Table 41). There were 5 species, varieties and forms, represented by very rare or rare specimens. TABLE 41. Results of microscopic examination of samples from the Mayam-Raf suite of the west coast of the Shmidt peninsula, northern Sakhalin (from the collection of O. S. Korotkevich, 1958) Sample no. cae Mis; CORRS aes | 100 99 98 Species 4 sandy-silty cla ye pee yaceey clay clay clay Dictyocha fibula Ebr. var. fibula fo fibulas soe Gees on Fe eee 1 - 2 2s — D. f. var. pentagona Schulz... . _ 1 — — — => Distephanus speculum (Ehr.) Hack. Vals (SPECWIUR: «.\rs..-9 4° 1 -— 1 1 1 D. s. var. pentagonus Lemm. . . 1 — _ — 1 =. Paradictyocha polyactis Freng. f{. po- Ts ee | ER ee toe 1 -- — 1 = Dictyocha fibula Ehr. var. fibula f. fibula predominates in all samples except 98 and 105. The varieties of Distephanus speculum (Ehr.) Hack. are either absent (samples 100 and 110) or appear as isolated skeletons. Two samples (100 and 115) contain isolated skeletons of Paradictyvocha polyaetis = 4 4 3 1 >) i} 2 D. s. var. cannopiloides (Pr.-Layr.) GL OSON settle he ch ate wes. ee — —_ 1 1 — _ = — = D. s. var. pentagonus Lemm. 1 — 1 2 —_ = = — tad D. s. var. septenarius (Ehr.) Jorg. | — | — | — = = > egies tal aa ats l= 1 hadi Ha ta mu 1° = o & Hales gess|s 2 |e = 1s ae [ts tq seek! seesles|ss|ssisz lez ZXQSR BAR BSIE SION |S 8 tg BIS 1 Vallacerta hortoniti Hanna| 1 2 { 5 2) 1 5 1 2 V. simplex Jousé . — 1 = = _ 1 5 — 3 V. tumidula Gleser 1 — -- { _- 5 — — 4 | Lyramula furcula Hanna 5 4 5 5 — 5 5 2 5 | L. simplex Hanna . 3 1 1 2 1 1 1 1 6 | Cornua aculeifera Dell. -- — _ 1 1 7 | C. poretzkajae Gleser — 2 -- 2 — — 8 | C. trifurcata Schulz . 1 1 5 1 2 3 3 2 9 | Dictyocha archangelski- ana (Schulz) Gleser . . 4 I 140 | D. triacantha var. apicu- lata Lemm. f. apicu- i IT RRIRTAN apeN GOR emer OA (ME = 1 ia _ { 1 — fF 5) DS te “var.” “apiculate f. late-radiata Schulz. | — 1 1 1 _ — 2 _ 12 | D. t. var. inermis Lemm. fe finermts ome. es — 1 | -- — i — * Higher estimates of abundance are presented in Tables 46—58. Among the species of Cornua Schulz, only C. trifurcata Schulz occurs in all the samples, usually at a low density, except in the basin of the Leplya River. C.aculeifera Defl. and C. poretzkajae Gleser are in the rare category. The family Dictyochaceae Lemm. is represented by 2 species, both belonging to Dictyocha Ehr. — D. archangelskiana (Schulz) Gleser and D. triacantha Ehr. with the following forms: var. inermis Lemm. f. inermig, var.°apiculata Lemm. f. apiculata and f. late-radiata Schulz. Representatives of the Dictyochaceae Lemm. occur sporadically in amounts ranging from very rare to rare. The general character of the flora remains unchanged throughout the territory despite fluctuations in species composition and numbers of certain forms. In the northernmost locality — the basin of the Nes'-Yugan River — only Lyramula furcula Hanna is abundant, while L. simplex Hanna is encountered in greater amounts than elsewhere. Similarly, L.furcula Hanna is the only abundant species in the basin of the Nyais River. The complex of Leplya River is characterized not only by the abundance of L. furcula Hanna, but also the very frequent occurrence of Cornua trifurcata Schulz, which was not found in other areas. Moreover, the rare species C. poretzkajae Gleser is found in the basin of the Leplya. The flora of the Loz'va River near Pristan' is dominated by 2 species: Vallacerta hortonii Hanna and Lyramula furcula Hanna. The silicoflagellate flora of the Serov District is on the whole very poor. 171 Occasionally Vallacerta hortonii Hanna and Cornua trifurcata Hanna predominate over the remaining forms. Lyramula furcula Hanna and Vallacerta tumidula Gleser dominate the complex of the Verkhotur'e area, which also includes the rare species Cornua poretz- kajae Gleser. Large amounts of Lyramula furcula Hanna, Vallacerta hortonii Hanna and V. simplex Jousé occur in the area of the Bol'shoi Aktai. This is the only locality where the latter species was found in large numbers. The complex of the Poludennyi Aktai is relatively poor; Lyramula furcula Hanna and Cornua trifurcata Schulz are dominant forms but are never more than rare in occurrence. Because of the scarcity of material possible changes of the silico- flagellate flora of the eastern slope of the Urals during the Santonian- Campanian cannot be discussed. Closely similar silicoflagellate complexes were found in the examined part of the Slavgorod suite covering a depth of about 53 m in well 268 near Pristan' on the Loz'va (Table 12). A study of the Slavgorod suite of well 13 near Verkhotur'e at 1-m intervals showed no significant quantitative or qualitative changes in the silicoflagellate flora from bottom to top of the section (Table 18). A comparison of our data with those of Zhuze (1949a, 1951), Krotov and Shibkova (1961) and Krotov (1957a, b) concerning the eastern slope of the Urals shows that the Upper Cretaceous silicoflagellate flora is fairly uniform in kind and numbers; the families Vallacertaceae Defl. and Cornuaceae Gem. predominate everywhere, while species of Dictyochaceae occupy a subordinate position. The general nature of the flora is the same in the Turgai Gates — the southernmost location of Upper Cretaceous silicoflagellates (Krotov and Shibkova, 1961). The literature provides some additional information on the composition of the Upper Cretaceous silicoflagellate flora. Thus, Dictyocha furcata Jousé, described from Upper Cretaceous deposits of the Bol'shoi Aktai River as frequent, was not found in our material; isolated specimens of this silicoflagellate were found in the basins of the Nyais and the Pelym rivers (Krotov and Shibkova, 1961). In addition, Krotov and Shibkova reported very rare to rare specimens of D. triacantha Ehr. var. triacantha f. triacantha from the eastern slope of the Northern and Central Urals, but this form does not appear in our materials. Thus, the Upper Cretaceous silicoflagellate flora of the eastern slope of the Urals consists of 14 species and varieties. Some features of this flora are exposed by comparison with the above-mentioned floras of Poland and California. Table 45 shows that the Upper Cretaceous flora of the Urals includes mainly forms which also existed in the Upper Cretaceous of other areas. Thus, 14 of the 20 species and varieties described from the Upper Creta- ceous were encountered on the eastern slope of the Urals. The flora of the Urals has 7 species and varieties in common with the flora of Europe, and 4 in common with the Californian flora. One species, Vallacerta hortonii, is known from the Upper Cretaceous flora of all three regions. Pentagonal skeletons in this species predominate not only in the Urals, but also in Poland and California; tetragonal and hexagonal forms are very rare. The following features are specific to the flora of the Urals: 1) 4 silicoflagellate species (Vallacerta 160 172 161 162 simplex Jousé, V.tumidula Gleser, Cornua poretzkajae Gleser, Dictyocha furcata Jousé) appear to be endemic as they are reported only from the Urals; 2) several species and varieties described from the Upper Cretaceous of Europe (Dictyocha triacantha var. triacantha f. minor Schulz, D.deflandrei Freng., D. schulziana Defl.) and California (Vallacerta hannai Defl., Dictyocha quadralta Hanna) were not observed in the Urals; except for Vallacerta hannai Defl., all these forms belong to the family Dictyochaceae. The main difference between the floras of the Urals and Europe is that the dominant complex of the Urals consists entirely of members of the families Vallacertaceae Defl. and Cornuaceae Gem., while the Polish flora contains, in addition to Vallacerta hortonii Hanna, considerable numbers of Dictyocha triacantha Ehr. which is represented by many forms in Europe but occurs sporadically in the Urals and is repre- sented here by isolated or rare specimens of only a few forms (D. tria cantha Ehr. var. triacantha f. triacantha, var. apiculata Lemm. f. apiculata and f: laté-radiata Schulz, and D.t. var. inermis Lemm. f. inermis). The flora of the Urals resembles its Californian counterpart in the quantitative proliferation of the most characteristic species. In both cases, Vallacerta hortonii Hannaand Lyramula furcula Hanna are dominant and occur together with smaller amounts of L. simplex Hanna. On the other hand, the American flora includes large amounts of members of the family Dictyochaceae Lemm., Corbisema geometrica Hanna and Dictyocha quadralta Hanna, generally not observed in the USSR. Judging from the high proportion of common species, the dominant position of the primitive families Vallacertaceae Defl. and Cornuaceae Gem. and also the equal proportions of the skeletons of the various forms of Vallacerta hortonii Hanna, it can be assumed that environmental conditions in the seas of the Urals, Europe and California were very similar during the Upper Cretaceous. The exceptional supremacy of the most primitive of the known silico- flagellates is due to its older age (Santonian-Campanian) compared with the Californian flora (Maestrichtian). The exact age of the flora of the Gulf of Danzig is unknown. Analysis of the vertical distribution of the species occurring in the Santonian-Campanian of the eastern slope of the Urals indicates that this flora can be divided into 3 groups. The first group consists of forms confined to the Upper Cretaceous; these include all the species of Cornua Schulz, Vallacerta simplex Jousé, V. tumidula Gleser and Dictyocha triacantha var. apiculata f. late-radiata Schulz. In the second group are placed 3 species (Vallacerta hortonii Hanna, Lyramula simplex Hanna and L. furcula Hanna) characterized by very wide distribution in the Upper Cretaceous but represented in Paleocene deposits by a negligible amount of isolated skeletons, and thus having no practical significance. These two groups form the characteristic Santonian-Campanian complex of the eastern slope of the Northern and Central Urals (Figure 4). The silicoflagellate fossils of the third Upper Cretaceous group occur sporadically and as isolated specimens. Some of them (Dictyocha 173 triacantha: Ehr. var. triacantiha, warsapicuiata Lemm,. 7a, inermis Lemm. and D. archangelskiana (Schulz) Gleser) are more widespread in the Paleocene, while one species, D. furcata Jousé, is rare both in the Cretaceous and in the Paleocene. (161) FIGURE 4. Characteristic silicoflagellate complex of the Santonian-Campanian of the eastern slope of the Urals; 1—Vallacerta simplex Jousé (Zhuze, 1949a); 2—V. hortonii Hanna; 3—V. tumidula Gleser; 4-—Lyramula simplex Hanna; 5—L. furcula Hanna; 6 — Cornua poretzkajae Gleser; 7—Dictyocha triacantha var. apiculata f. late-radiata Schulz; 8—Cornua trifurcata Schulz, SILICOFLAGELLATES OF THE CENOZOIC Silicoflagellates of the Paleogene Paleogene silicoflagellates are known from the USSR, Western Europe, North America and New Zealand. Only a few comprehensive works have been published on the silico- flagellates of the Paleogene. Two articles are well known: one dealing 174 163 with the silicoflagellates of Western Siberia (Glezer, 1960), and the other with those of California (Mandra, 1960). The earliest silicoflagellates — those of the Paleocene — are known only from the USSR. Silicoflagellates of the Paleocene Publications on the Paleocene silicoflagellates concern two regions in the USSR — the Volga area and the eastern slope of the Urals. Schulz (1928) used materials from the Paleocene deposits of the Ul'yanovsk Region (former Simbirsk Province) in a study of the Systematics of silicoflagellates. This author found only 2 species — Dictyocha archangelskiana (Schulz) Gleser and D. triacantha Ehr. with several varieties and forms. The results of his research appear in the monograph by Gemeinhardt (1930). N. V. Anisimova‘obtained similar data with respect to the composition of the silicoflagellate flora of the lower Syzran deposits; beside diatoms, she found several varieties of D. triacantha Ehr. No special studies have been made of the Paleocene silicoflagellates of the eastern slope of the Urals. Silicoflagellate skeletons were encountered by Zhuze (1951), Krotov (1957a, b), and Krotov and Shibkova (1961) during studies of the diatom flora. D. triacantha Ehr. forms a considerable portion of the dominant upper complex of the Early Paleocene (Krotov, 1957a) or the Late Paleocene complex (Krotov, 1957b). The characteristic complex of the Early Paleo- cene of the eastern slope of the Urals has been described (Glezer, 1960). TABLE 47. Distribution of silicoflagellates in the Early Paleocene of the eastern slope of the Urals Makhnevo area Species i= ) ~ =| E o 2 = S o oS eG a 4 nn 4 nm a the Loz'va River interfluve ofthe Tura and Tagil +3) ey “— = 5 $ a ° A 3 > x fo) g 5 n > Ivdel' area Kokui sector — — | Vallacerta hortonii Hanna .... . — 2 Lyramula furcula Hanna. .... . — 1 _ _ _ 1 3 BesimplexsHannials! kh 2° 2. wines tee — 4 = — = = 4 Dictyocha archangelskiana (Schulz) GI GSGRe ate tte oeca tae cee Lees 1 2 1 _ 1 3 a DD: furcata: LOUSe. IST I WISN « — _ — — 1 1 6 D. triacantha Ehr. var. triacantha f. PRIGCUMLNG..7. ergata. Cores Gere ea: — 1 — — 2 3 7 D. t. var. apiculata Lemm. f. apicu- atin: come isd sets SE AL Si 1 1 — -— 1 2 8 D. t. var. apiculata f. minor Schulz 2 3 1 1 Z 4 9 ID? tt Var. hastata’ Lemme 2. 2° 2 5 1 5 5 5 10 D. t. var. inermis Lemm. f. inermis 2 1 1 — 3 4 11 D. t. var. inermis f. minor Gleser. . 2 4 1 4 2 D 12 Mesocena aff. apiculata (Schulz) Def}. it 2 2 _ 2 3 175 In addition, an Early Paleocene silicoflagellate flora has been found in the following parts of the eastern slope of the Northern and Central Urals: the Ivdel' area (wells 361, 564), the Serov District (well 459, Sosva line) and the Makhnevo area (wells 90, 547, 1482, 1503) (Table 47). Several silicoflagellate-containing samples from the Volga area are given for comparison. In the areas studied in the eastern slope of the Urals, a total of 12 species, varieties and forms of silicoflagellates were found. These belong to 4 genera (Lyramula Hanna, Vallacerta Hanna, Dictyocha Ehr. and Mesocena Ehr.) and 3 families (Vallacertaceae Defl., Cornuaceae Gem. and Dictyochaceae Lemm.). Representatives of Dictyochaceae Lemm. exceed by far, numerically and qualitativelly, those of the other 2 families; on the other hand, species of Cornuaceae Gem. are very rare and occur as isolated specimens. The family Dictyochaceae includes 4 species in this flora; 3 of these belong to the genus Dictyocha Ehr. (D. archangelskiana (Schulz) Gleser, D. furcata Jousé and D. triacantha Ehr.) and one to the genus Mesocena Ehr. (M. aff. apiculata (Schulz) Defl.). Most characteristic of all areas is the exceptionally polymorphic species Dictyocha triacantha Ehr., whose 6 varieties and forms differ morphologically considerably from one another. D. triacantha var. hastata Lemm. is most abundant in almost all areas; var. inermis f. minor Gleser, var. inermis Lemm. f. inermis and var. apiculata f. minor Schulz occur everywhere in smaller amounts; var. apiculata Lemm. f. apiculata is ubiquitously present ina small number of specimens; rarest of all is D. triacantha Ehr. var. triacantha f. triacantha. D. archangelskiana (Schulz) Gleser and Mesocena aff. apicu- lata (Schulz) Defl. are fairly widespread but not abundant. Dictyocha furcata Jousé can be regarded as a rare species, since it is represented in the Makhnevo area only in very rare numbers. The floras of the Northern and Central Urals are almost identical in species composition and in degree of abundance. On the whole, the density of silicoflagellates increases steadily during the Early Paleocene (Figure 2). Of all the silicoflagellate species and varieties, however, only D. tria- cantha var. hastata Lemm. shows a steady rise in density in the course of time. This feature is of particular interest since var. hastata is the only silicoflagellate with a bilaterally symmetrical skeleton during the Paleocene, while all the other forms possess radially symmetrical skeletons. The latter feature can be regarded as an indication of the more primitive structure of the skeleton in the family Dictyochaceae Lemm. The density of silicoflagellate skeletons in Paleocene deposits of the eastern slope of the Northern and Central Urals was used by Krotov (1957a, b) as a feature distinguishing between dominant lower (Early Paleocene) and upper (Late Paleocene) complexes. According to Krotov, the earlier complex shows a poor silicoflagellate development, while the later complex contains large amounts of silico- flagellate skeletons. This observation, however, does not agree fully with our data or with the lists published by Krotov and Shibkova (1961). 164 165 176 (164) FIGURE 5. Characteristic silicoflagellate complex of the Early Paleocene of the eastern slope of the Urals; 1—Dictyocha triacantha var, inermis f. minor Gleser; 2—D.t. var. inermis Lemm, f. inermis; 3—D. archangelskiana (Schulz) Gleser; 4 — Ditriacantha Ebr, var triacantha £ triacantha: 5—D. t. var, hastata Lemm.; 6—D. t. var. apiculata Lemm. f. apiculata; 7—D. t. var. apiculata f. minor Schulz. A comparison of our results with those of Krotov and Shibkova (1961) and Krotov (1957a, b) leads to the conclusion that the abundance and system- atic composition of the silicoflagellate flora of the Early Paleocene were roughly uniform on the eastern slope of the Urals from the Ust'- Man'ya River in the north to the Kamyshlov area in the south. Nevertheless, our materials show a greater variety of forms compared to those of Krotov, probably because of the more detailed determination. In the study of the Early Paleocene silicoflagellates of the Volga area we used materials from the Penza and Ul'yanovsk regions (Table 48). 177 166 TABLE 48, Distribution of silicoflagellates in the Early Paleocene of the Middle Volga area 1 Dictyocha archangelskiana (Schulz) Gleser_ . — 1 2 D. triacantha Ehr. var. triacantha f. tria- CONUS, - RR oo RE > ye 4 4 3 D. t. var. apiculata Lemm. f. apiculata 1 2 4 D. t. var. apiculata f. minor Schulz 4 2 5 D. t. var. inermis Lemm. f. inermis 1 il 6 D. t. var. inermis f. minor Gleser — 1 7 Dei var. astata GCMs Se. os) tak Sens 4 4 Seven varieties and forms of 2 species of Dictyocha Ehr. of the family Dictyochaceae Lemm. were determined. More widespread and abundant is the polymorphic species D. triacantha Ehr. with its 6 varieties and forms. Some of these forms appear at high density (var. hastata Lemm., var. triacantha f. triacantha, var. apiculata f. minor Sena, while others are very rareorrare (var. apiculata Lemm. f. apiculata var. inermis Lemm. f. inermis andf. minor Gleser). D. tria- cantha var. hastata is the most widespread of all, and was encountered in almost all localities examined. D. archangelskiana (Schulz) Gleser is one of the rarest species. Only one form mentioned in the literature can be added to this list, namely, D. triacantha var. triacantha f. minor Schulz found by Schulz (1928) and Gemeinhardt (1930) in the Paleocene of Ul'yanovsk (Simbirsk). The lack of quantitative data in these two publications prevents a more detailed comparison. The three varieties of D. triacantha Ehr. determined by Anisimova (var. triacantha, var. apiculata:Lemm.,. and var. hHastata Lenuma) occurs as isolated specimens. Thus, the same varieties and forms of D. triacantha Ehr. pre- dominate in the Early Paleocene floras of the Volga area and the Urals, although their density in the Urals is greater than along the Volga. The only exception to this is D. triacantha var. triacantha Ehr. f. triacantha, whichappears tobe more abundant in the Volga area. However, D. triacantha var. hastata Lemm. is the most widespread form in both regions. The following species occur in the Urals, but not in the Volga area: Dictyocha furcata Jousé, Mesocena aff. apiculata (Schulz) Defl., Vallacerta hortonii Hanna, Lyramula*furculay Hanae and L. simplex Hanna. However, all these species, except for Meso- cena aff. apiculata (Schulz) Defl., occur sporadically and as isolated specimens in the Urals. Thus, the characteristic Early Paleocene complex of the eastern slope of the Urals consists of the following silicoflagellates: Dictyocha triacantha Ehr. withits varieties and forms (var. hastata Lemm., var. apiculata Lemm. f. apiculata andf. minor Schulz, var. inermis Lemm. f. inermis andf. minor Gleser, var. triacantha f. triacantha), D.archangelskiana (Schulz) Gleser, and Meso- cena aff. apiculata (Schulz) Defl. (Figure 5). 178 167 168 This similarity between the floras of the Volga area and the eastern slope of the Urals proves their contemporaneous occurrence and indicates that the European and eastern Ural seas were linked during the Early Paleocene. The Early Paleocene flora evolved from the Upper Cretaceous flora. All Early Paleocene elements are known from the Cretaceous, except for Mesocena aff. apiculata (Schulz) Defl.,. Dictyocha triacantha var. inermis f. minor Gleser and, probably, var. hastata Lemm. Nevertheless, the Early Paleocene flora differs sharply from that of the Cretaceous since it is dominated by the family Dictyochaceae Lemm., which occurs only rarely in the Upper Cretaceous. On the other hand, such typically Cretaceous families as Vallacertaceae Defl. and Cornuaceae Gem. are rare in the Early Paleocene, indicating that they were becoming extinct. Silicoflagellates of the Eocene-Oligocene The silicoflagellates of the Eocene (and probably also the Oligocene) have been studied in Western Europe, the European part of the USSR, Western Siberia, California and New Zealand. The Early Eocene silicoflagellates of Denmark were investigated by Lemmermann (1901b), Schulz (1928), Gemeinhardt (1930), Deflandre (1932a, b, 1950) and Frenguelli (1940). Gemeinhardt (1930) published a study of the Early Eocene silicoflagellates of northern Germany. All these authors deal exclusively with the classification of silicoflagellates. Consequently, their works provide only a general idea of the systematic composition of the Early Oligocene silicoflagellate flora. Only Deflandre (1932a) lists the silicoflagellates found on Fuur Island (Denmark), but like the other works, this article lacks quantitative data. On the basis of the work of these authors, it can be concluded that the Early Eocene flora of northern Germany and Denmark consists entirely of members of the family Dictyochaceae — Dictyocha Ehr., Navicu- lopsis Freng. and Distephanus Stohr. The genus Dictyocha Ehr. is richest in species, some of which (D. triacantha Ehr., D. fibula Ehr.) are highly polymorphic. Table 49 includes a combined list of Early Eocene silicoflagellates found by these authors in Denmark and northern Germany. Only 2 silicoflagellate species — D. staurodon Ehr. and Navicu- lopsis biapiculata (Lemm.) Freng. — are known from the Eocene of the Bay of Ahus in southern Sweden. Cleve-Euler and Hessland (1948) place the diatom and silicoflagellate floras they found in the Early Eocene because of the similar generic composition of the Danish flora and that of the Bay of Ahus. Zhuze (1952) considers the Swedish diatom flora to be of Late Eocene age because of its similarity to the Late Eocene diatom flora of Western Siberia. Eocene silicoflagellate flora is found in the USSR in the Volga area and Western Siberia. In the Volga area, most authors (Schulz, 1928; Gemeinhardt, 1930; Deflandre, 1932a, b, 1950; Frenguelli, 1940) studied the silicoflagellate flora of Kuznetsk. Zhuze (1949b) places the diatom flora of Kuznetsk in 179 the Early Eocene. In addition, Deflandre (1950) investigated the silico- flagellates of the Eocene of the towns of Sengilei, Kamyshin, etc. (167) TABLE 49. Distribution of silicoflagellates in the Early Eocene of Europe and Asia : Western Western No. Species Bukope Volga area Siberia 1 | Dictyocha archangelskiana (Schulz) Gleser . — = an 2 | D. deflandrei Freng. var. deflandrei -f oo + 3. | D. d. var. completa f. producta Gleser . = a5 ze 4 = elata Gleser var. elata . = s 2. =>. 6 + — a D+ |). telongatasGleser wo OL SLL 2 SRS — +- + 6 | D. fibula Ehr. var. fibula f. fibula... . +- at ae 7 | D. f. var. fibula f. eocaenica Krotov .. . + + = 8 | D. f. var. fibula f. rhombica Schulz 4- ao + 9 | D. f. var. fibula f. rotundata Schulz . . . -— of = 40) | D: jf: vate pentagona Schulz ... . .< + — = 14 | D. frenguellii Defl. var. frenguellii . . . . —_ ++ — 12 | D. f. var. carentis f. incerta Gleser. . . . = + = 13 | D. lamellifera Gleser var. lamellifera . . . + + 14 | D. 1. var. constricta Gleser ....... — +- “f- 15°] Dt, vars hastateGleser 2°: 2. 4LP. — + 4 AG. oh aaa ieee ee Be ec sc wh munceh -+ -+ + 17 | D. staurodon Ehr. f. staurodon. .... . -|- — —_— 48% UD? svi? minertschiulzss qs ek. 207 8G +- + = 19 |B: transitoria Well feces, os tiee Pon Aue — -}- — 20 | D. triacantha Ehr. var. triacantha f. tria- cantha +), (SI AAO ID Boa + + — 21 | D. t. var. triacantha f. minor Schulz. -f- — — 22 | D. t. var. apiculata Lemm. f. apiculata. . 4- + 4. 23 | D. t. var. apiculata f. minor Schulz 4 -f i 24 5) (D> vary hasteta, Lemme.) babes Lk. + +- + 25 | D. t. var. inermis Lemm. f. inermis -+ a —— 26 | D. t. var. inermis f. minor Gleser os — — + 27 | Distephanus crux var. mesophthalmus (Ehr.) TACT AT ae op hace ce a Rie hn ee ee oe a — oa 28 | D. speculum var. pentagonus Lemm. : — — += 29 | D. s. var. septenarius (Ehr.) Jorg. . . . . + -- — 30 | Naviculopsis biapiculata (Lemm.) Freng. var. PIAPLCUIAUE? nce carr emer ie oa ae aim =F 31 N. b. var. constricta (Schulz) Gleser. . . . — + -= 32 | WN. b. var. minor (Schulz) Gleser. . . . . + +: Sin aor | wasroousia Dell. . . 4 < s . so™ 2. —_— + + 34 | N. trispinosa (Schulz) Gleser. . ..... ++ — — 30. | Mesocena circulus Ehr. . .... 0°... + + — These publications dealing with the Eocene of the Volga area as well as that of Denmark and northern Germany, relate only to systematic composi- tion of the silicoflagellate flora. All the silicoflagellates encountered belong to 3 genera of the family Dictyochaceae Lemm.: Dictyocha Ehr., Naviculopsis Freng. and Mesocena Ehr. The genus Dictyocha Ehr. appears to contain the largest number of species. D. triacantha Ehr., D. fibula Ehr. and Naviculopsis biapiculata (Lemm.) Freng. show a considerable degree of variation in this flora. In Western Siberia deposits which contain abundant diatom and silico- flagellate fossils were studied from the Early, Middle (?) and Late Eocene and from the Late Eocene— Early Oligocene (?). The first report (Zhuze, 1955) on the Eocene — Early Oligocene silicoflagellates of Western Siberia contained descriptions and drawings of several silicoflagellate species, including one new to science. Many students of the diatom flora of Western Siberia also determined silicoflagellates. A number of silicoflagellates 180 from Early Eocene deposits are mentioned by Krotov (1957a, b) and Krotov and Shibkova (1961) for the eastern slope of the Urals and of the Trans- Urals, and by Rubina (Rudkevich, Rubina and Fermyakov, 1957) and Galerkina (1959) for northern parts of the West Siberian plain. A few silicoflagellates participate together with the diatoms in the dominant complexes of the Middle (?) Eocene of the West Siberian plain (Rudkevich, Rubina, Permyakov, 1957; Galerkina, 1959; Strel'nikova, 1960). More- over, silicoflagellates have also been reported as components of the Late Eocene and Late Eocene — Early Oligocene (?) complexes of the northern part of the West Siberian plain (Rudkevich, Rubina and Permyakov, 1957; Galerkina, 1959; Strel'nikova, 1960), the eastern slope of the Urals and the Trans-Urals (Krotov, 1957a, b; Krotov and Shibkova, 1961), the areas of the settlements of Kuznetsovo, Luchinkino, Kamensko-Gusel'nikovo, Lar'yaka, the cities of Omsk and Tyumen! (''Stratigrafiya Mezozoya..., etc.,'' 1957), the settlements of Tara and Uvat, the town of Khanty- Mansiisk, the basin of the Khadyr-Yakha, and the Pavlodar Region (Vozzhennikova, 1960). Most of the silicoflagellates found in the Eocene and Eocene — Oligocene (?) are various species, varieties and forms of the genus Dictyocha Ehr. The article by Glezer (1960) deals with the characteristic silicoflagellate complexes of the various subdivisions of the Eocene and Early Oligocene (?) of the eastern slope of the Urals and the West Siberian plain. Only a few works deal with Eocene silicoflagellates of California. Hanna (1931) gives only drawings of a few species he found in the diatomites of the Krayenhagen formation of the San Joaquin valley. Hanna places these diatomites with reservation in the Late Eocene, although he does not rule out an Early Oligocene origin. Some of these silicoflagellates were encountered by Clark and Campbell (1945) in the lower part of the Krayenhagen formation, whose radiolarian fauna was named Late Eocene. Mandra (1960) made a special study of the silicoflagellates of the Late Eocene of the Mount Diablo area in California (Kellogg and Sydney slates). He prepared a list of the Late Eocene silicoflagellates and compared the Late Eocene silicoflagellate flora with the Cretaceous and Neogene complex- es of California. According to Mandra, the most characteristic silicoflagellates of the Late Eocene of California are Corbisema apiculata (Lemm.), C. triacantha (Ehr.) (both of which appear to be identical to Dictyocha triacantha Ehr.), Distephanus variabilis Hanna (= the varieties of D. speculum (Ehr.) Hack.), Mesocena oamaruensis Schulz and Naviculopsis biapiculata (Lemm.) Freng. The silicoflagellates of the Late Eocene (Kanaya, 1957), Late Eocene— Early Oligocene (Fleming, 1959) or Early Oligocene (Deflandre, 1950) diatomites of New Zealand have been used in studies of silicoflagellate taxonomy (Schulz, 1928; Gemeinhardt, 1930; Frenguelli, 1940; Deflandre, 1950), but relate only to the systematic composition of the silicoflagellates of Oamaru, New Zealand. All the silicoflagellates described there belong to the genera Dictyocha Ehr., Naviculopsis Freng., Distephanus Stohr and Mesocena Ehr. Most of the species, varieties and forms belong to the genus Dictyocha Ehr. 181 Silicoflagellates of the Early Eocene Ezrly Eocene silicoflagellate flora was examined by us in many areas of the eastern slope of the Urals, Trans-Urals, and the Volga area. Moreover, these materials were compared with a sample from Early Eocene deposits of Mors Island, Denmark. Early Eocene silicoflagellates are known from the following parts of the eastern slope of the Urals and the Trans-Urals: Ivdel' area (Northern Urals), the areas of Serov and Alapaevsk (Central Urals), Vogulka River (Berezovo area) and Taz peninsula in the basin of the Srednaya Khadyta. The results of this study appear in Table 50. (170) TABLE 50, Distribution of silicoflagellates in the Early Eocene of the eastern slope of the Urals and the Trans-Urals Srednaya Khadyta River Species 1 | Dictyocha archangelskiana (Stliaiz)"Gleser nae... — 1 1 — _ D. deflandrei Freng. var. de- [landrels s.. 1m. tests. — — D. elongata Gleser ..... 2 1 D. fibula var. fibula f. eocae- nica KOO Sc ane eek aes 1 D. lamellifera Gleser var. la- MEW IETE by Wet sty El hoale ste D. l. var. constricta Gleser D. 1. var. hastata Gleser. .. Der napicnlar ne, cone vecetes D. triacantha Ehr. var. tria- cantha f. triacantha . .. . — 2 _ — _ D. t. var. apiculata f. minor Sebulz, ie esas see. — 1 1 1 _ D. t. var. inermis Lemm. Ie METIS woh ge mea 1 1 1 1 -— D. t. var. inermis f. minor Glesery og SRETES. s, fonns. 3. 3 1 _ — 1 1 D. t. var. hastata Lemm. . . — 1 1 1 1 Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata . . 1 1 -— 1 4 N. b. var. minor (Schulz) Gle- _— O_O Db = CO OOND 1 FO WW |wnwn m | oreo as —_—s HS GO — on _ a> = = | So ia) & n” ~ 8 o oO lene) = _ bt re) NO It appears from the table that Early Eocene silicoflagellate flora numbers 16 species, varieties and forms belonging to 2 genera; Dictyocha Ehr. and Naviculopsis Freng. of the family Dictyochaceae Lemm. Most of the silicoflagellates (7 species with 13 varieties and forms) belong to Dictyocha Ehr., and only 2 species belong to Naviculopsis Freng. The dominant position is held exclusively by species of Dictyocha Ehr. The varieties of the polymorphic species D. lamellifera Gleser (var. lamellifera, var. constricta Gleser and var. hastata Gleser) are abundant almost everywhere, as is D. fibula var. fibula f. eocaenica Krotov. The other species of Dictyocha (D. elongata Gleser and some forms of D. triacantha Ehr.) occur in almost all the 182 170 71 localities but at moderate density. Finally, D. archangelskiana (Schulz) Gleser, D. deflandrei Freng. var. deflandrei and D. navicula Ehr. can be characterized as rare. Species of Naviculopsis Freng. appear at a fairly low density. Only one species — N. robusta Defl. — shows an almost ubiquitous distribution; varieties of the other species, N. biapiculata (Lemm.) Freng., occur very rarely. The species compositions of complexes of different parts of the Northern and Central Urals are almost identical, and the differences observed concern mainly the numbers of some forms. Silicoflagellates are scarce on Taz peninsula. In order to trace changes in the silicoflagellate flora during the Early Eocene, a series of samples from a 70-m layer of Early Eocene diatomites from well 564 inthe Ivdel' area were examined. No significant modification of the flora could be detected from the bottom to the top of the examined interval (Figure 3), except for the disappearance of skeletons of Dictyo - cha elongata Gleser and D. triacantha var. apiculata f. minor Schulz from the upper part of the layer, the appearance of Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata anda slight increase in the density of Naviculopsis robusta Defl. These changes are too negligible to lead to any conclusions. It is often difficult to compare our results with the data published in the literature on Early Eocene silicoflagellates of the eastern slope of the Urals and the West Siberian plain (Krotov, 1957a, b; Rudkevich, Rubina and Permyakov, 1957; Galerkina, 1959). This is due to the scarcity of diagnoses and drawings, which frequently makes it impossible to decide whether two authors are speaking of the same or different forms. It was, nevertheless, possible to compare our observations with those of Krotov and Shibkova (1961), who published drawings of some forms. There is full agreement between our data and those of Krotov and Shibkova with respect to the density and distribution of the following silicoflagellates on the eastern slope of the Northern and Central Urals: Dictyocha archan- gelskiana (Schulz) Gleser (=Corbisema geometrica Hanna),* D. lamellifera var. constricta Gleser (=D. triacantha f. eocaenica Krotov), D. triacantha var. inermis f. minor Gleser (=D. triacantha var. apiculata Lemm.), Naviculopsis bi- apiculata (Lemm.) Freng. (=Dictyocha biapiculata Lemm.), N. robusta Defl. (=Dictyocha biapiculata f. eocaenica Krotov). It must be mentioned that only one form — Distephanus speculum var. pentagonus Lemm. — was found as isolated specimens in the samples from some parts of the eastern slope of the Northern and Central Urals by Krotov and Shibkova, but not by us. We examined Early Eocene silicoflagellate flora of the Volga area in samples from 3 points in the Ul'yanovsk Region (the towns of Sengilei and Akhmetlei and Sharlovo village). A total of 9 species of 2 genera (Dictyocha Ehr. and Naviculopsis Freng. of the family Dictyo- chaceae Lemm.), which were represented by 20 varieties and forms, were determined. The genus Dictyocha Ehr. showed the largest variety, being represented by 7 species with 16 varieties and forms. * The determinations of Krotov and Shibkova are given in parentheses, 183 172 TABLE 51. Distribution of silicoflagellates in the Early Eocene of the Middle Volga area Sharlovo —= Dictyocha deflandrei Freng. var. defland- | RR IE Te Ak Sp rnd i Tali Dh Nea 2 1 1 2) DD. elongate (Glesert © 4.45 6) 02 1 _ 2 3 | D. fibula var. fibula f. eocaenica Krotov 3 1 2 4 |D. f. Ehr. var. fibula f. fibula fe 1 = af 5 |D. f. var. fibula f. rhombica Schulz . . 3 _ — 6 |D. lamellifera Gleser var. lamellifera. . 2 2 5 7 +|D. Ul. var. constricta Gleser ...... 5 1 2 S TD. t Vale asta Olesen.) |. eRe Pee 1 — 1 Oa Pies ep ierla te iames. 5 cee iindie ae seek i — — Oe Ea rramsz ori MDM oes cous os cn ny ym cy © 1 — - 11. | D. triacantha Ehr. var. triacantha f. tria- CORI OR. EW es TAR! Seay 2 1 1 12 D. t. var. triacantha {. minor Schulz. 1 — _ 13. | D. t. var. apiculata Lemm. f. apiculata 1 1 1 14 | D. t. var. apiculata f. minor Schulz . . 2 1 _- 4s HED. 9%. VAR asta a SCM m2 wean a. pens 1 1 4 16 |D.t var. inermis Lemm. f. inermis . . { — — 17 |D. t. var. inermis f. minor Gleser . . . 1 — _ 18 | Naviculopsis biapiculata (Lemm.) Freng. VOL DiGPICpAGhs Sy ees os ny ty 1 = 19 | N. b. var. minor (Schulz) Gleser 3 20s [WN robusta sei? . fre) wa. 2s < p) Here, the genus Naviculopsis Freng. consists of only 2 species, one with 2 varieties. The only abundant silicoflagellates are some representatives of Dictyocha Ehr., while species of Naviculopsis Freng. occur at a lower density. Two complexes can be distinguished on the basis of the qualitative and quantitative composition of the flora. The older complex of the town of Sengilei and Sharlovo village is characterized by the abundance of var. lamellifera orvar. constricta Gleser of D. lamellifera Gleser and the presence of small amounts of D. elongata Gleser, D. fibula var. fibula f. eocaenica Krotov and Naviculopsis robusta Defl. All these silicoflagellates are typical of the Early Eocene of the eastern slope of the Urals. Although it is very poor, the silicoflagellate flora of Akhmetlei re- sembles the older complex described above in the predominance of Dictyocha lamelliféra Gleser var! lamelMifeéera. In the younger complex of Sengilei, D. fibula Ehr. var. fibula f. fibula andf. rhombica Schulz and Naviculopsis biapiculata var. minor (Schulz) Gleser predominate, while characteristic forms of the older complex are almost completely absent. Comparison with the data published in the literature shows that this complex is similar in composition to the silicoflagellate flora of the town of Kuznetsk, and have in common a considerable number of species and forms (Dictyocha deflandrei Freng. var. deflandrei, D. fibula Ehr. var. fibula f. fibulaandti? rhombica Schulz, D. transiiorre Defl.; D. tria‘cantha Hhri vars triacantha ft riacantma rane varieties of Naviculopsis biapiculata (Lemm.) Freng.). No quantitative information on the Kuznetsk flora was published. 184 173 In preparation 167 of the dried diatom collection of Cleve and Moller from Mors Island in Denmark, we determined 5 silicoflagellate species and varieties belonging to Dictyocha Ehr. and Naviculopsis Defl. of the family Dictyochaceae Lemm. Naviculopsis biapiculata (Lemm.) Freng. predominates in this flora, while other forms (Dictyocha deflandvei Wreng. varmdeflandre:t, D. navicula,Ehr-.;.D. triacantha var. hastata Lemm. and var. inermis Lemm. f. inermis) appear at a low density. Table 49 represents a combined list of the silicoflagellates occurring in the Early Eocene of Western Europe, the Volga area and the eastern slope of the Urals based on our own and published observations. Of all the silicoflagellate species, varieties and forms known at present from the Early Eocene, 17 have been found on the eastern slope of the Urals. More than half of these (10) were also encountered in both the Volga area and in Western Europe, 4 forms are shared with the Volga area only, while 3 are known only from the Early Eocene of the eastern slope of the Urals and the West Siberian plain. Skeletons of several forms (D. elata Gleser var. elata, D. freng- wellii Defi; war. frengucéilii amd vary carentys f. incerta Gleser, D. transitoria Defl.) known from the Early Eocene deposits of Western Europe or the Volga area, but not found in contemporaneous deposits of the eastern slope of the Urals or the West Siberian plain were only encountered in these two areas in more recent strata. The Early Eocene flora of the eastern slope of the Urals closely re- sembles the older Early Eocene complex of the Volga area both in species composition and in the quantitative relations of the forms. The characteristic Early Eocene complex of the eastern slope of the Urals and of the Trans-Urals consists of the following silicoflagellates (Figure 6): Dictyocha lamellifera Gleser var. lamellifera Doi. var..constricta Gleser Dl. vary tWastata Gleser D. fibula var. fibula f. eocaenica Krotov D. elongata Gleser D. navicula Ehr. Naviculopsis robusta Defl. The second, younger complex of the Early Eocene flora of the Volga area resembles more closely the contemporaneous Early Eocene flora of Western Europe in the presence of relatively large amounts of D. fibula Ehr. var. fibula f. fibula andf. rhombica Schulz and Naviculop- sis biapiculata (Lemm.) Freng. On the whole, the flora of the Urals and the more ancient complex of the Volga area are more primitive because of the predominance of triangular forms of Dictyocha lamellifera Gleser (related to the ancient species D. triacantha Ehr.) and the presence of a primitive species of Naviculopsis —N. robusta Defl. The younger complex of the Early Eocene of the Volga area and the flora of Western Europe probably reflect the next stage in the formation of the flora. All the above statements indicate that the older Early Eocene complex was first formed during more or less similar conditions in the European and Siberian marine basins. 185 FIGURE 6. Characteristic silicoflagellate complex of the Early Eocene of the eastern slope of the Urals and the Trans-Urals; 1—Dictyocha lamellifera Gleser var. lamellifera; 2—D. l. var. constricta Gleser; 3—D. 1. var. hastata Gleser; 4—Naviculopsis robusta Defl.; 5—Dictyo- cha elongata Gleser; 6—D. navicula Ehr.; 7—D. fibula var. fibula f. eocaeni- ca Krotov. The Early Eocene flora differs sharply from the known Early Paleocene flora in possessing several new species and even 2 new genera — Navi- culopsis Freng. and Distephanus Stohr. Silicoflagellates of the Middle (?) Eocene Results of the examination of Middle Eocene silicoflagellate flora of the southern part of Taz peninsula, as well as the Sherkaly settlement and the areas of Ivdel' and Serov on the eastern slope of the Northern and Central Urals are given in Table 52. The table shows that a total of 17 silicoflagellate species, varieties and forms are known from the Middle (?) Eocene. These are distributed among the genera Dictyocha Ehr. and Naviculopsis Freng., both of the family Dictyochaceae Lemm. Most of the forms (14) belong to Dictyocha Ehr., while fewer (3) belong to Naviculopsis Freng. Dictyocha frenguellii var..carentis Gleser!l. carenten and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata are the most widespread and were encountered in all areas. The latter usually occurs at a lower density. In addition, Dictyocha lamellifera Gleser var. lamellifera is almost universally encountered. 174 186 175 TABLE 52. Distribution of silicoflagellates in the Middle (2?) Eocene of the eastern slope of the Urals and the West Siberian plain Taz peninsula Lower |Eastern slope of Obarea} the Urals o st a a 3 = w ~ =I < 3 6 = 3 a s TS "oy, v ; idee tecdccsa se eel pee oO No. Species = Y = > idee 2 ra o co Zo]o 6 = ' o MG =< o v 0] et Pa ee ee 8. |. Soh Bl g > ke u Ss aN ae don (SS = a = uJ Fo ges oy Soe a & = — > 3 & dls re Meg lee me o re) 4 a > oO ee) a cs) Oo ta Ls Ge = at es sc a > (3) GY gee 5 5 D. lamellijera Gleser var. lamellifera .. . 1 4 ye 3 2 2 — D. navicula Ehr. .. . — — D. triacantha Ehr. var. triacantha f. triacantha | — 2 _ 2 1 — 4 — 10 |D. t. var. apiculata Lemm. f. apiculata — — _— — _ — 1 44 | D. t. var. apiculata f. mi- norschulz” Fee : 1 1 1 3 — — a 1 12 | D.t. var. hastata Lemm. | — = -- - 4 _ — 3 13 | D. t. var. inermis Lemm. [i imermis : B «es oe: _ — ~~ — -- ~— — 4 44 |D. t. var. inermis f. mi- norsGleser Tao Eee — — 1 2 4 — 1 15 | Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata ..... 4 2 1 3 4 1 1 1 46 | N. b. var. minor (Schulz) Gleser 2. so 47 | WN. robusta Defl. . ..]| — _ — — _ — — wh ns —= on = tw te ot co CO ~ lop) on = OO _ on _ on | | | = DO D. elata Gleser var. elata, some varieties of D.triacantha Ehr. and Naviculopsis biapiculata var. minor (Schulz) Gleser have a more limited range and occur in some localities only. The category of rare silicoflagellates include Dictyocha elongata Gleser, D. fibula var. fibula f. eocaenica Krotov, D. navicula Ehr. and Naviculopsis robusta Defl. The floral complexes of these areas differ from one another in species composition and especially in the quantitative proportions of the elements. Thus, the flora of the Arka- Tab-Yakha Basin is rich in 3 forms — D. frenguellii var. carentis Gleserf. carentis, D. elata Gleser var. elata and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata. The dominant complex of the basin of the Khadutta River consists of abundant amounts of D. lamellifera Gleser var. lamelli- fera and Naviculopsis biapiculata var. minor (Schulz) Gleser in addition to D. frenguellii var. carentis Gleserf. carentis. 187 The flora of the En-Yakha River is dominatedby Dictyocha frenguellii var. carentis Gleserf. carentis and Naviculopsis biapiculata var. minor (Schulz) Gleser, which occur together with considerable amounts of Dictyocha lamellifera Gleser var. lamellifera, D.elata Gleser var. elata, D. triacantha var. apiculata f. minor Schulz and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata. Only Dictyocha frenguellii var. carentis Gleser f. carentis occurs in frequent numbers in the Ivdel' area. The silicoflagellate flora of the Serov area is slightly more abundant; D. frenguellii var. carentis Gleserf. carentis occurs here in large numbers, while D. triacantha var. inermis f. minor Schulz, D. lamellifera Gleser var. lamellifera and D. fibula Ehr. var. fibula f. fibula are less abundant. The Serov flora also includes rare forms such as D. elongata Gleser, D. navicula Ehr., D.triacantha var. inermis Lemm. f. inermis andvar. apiculata Lemm. f. apiculata and Naviculopsis robusta Defl. FIGURE 7. Characteristic silicoflagellate complex of the Middle (?) Eocene of the eastern slope of the Urals and the West Siberian plain; 1,2—Dictyocha frenguellii var. carentis Gleser f. carentis; 3—D. elata Gleser; 4— Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata; 5—N. B. var. minor (Schulz) Gleser; 6— Dictyocha lamellifera Gleservar. lamellifera. 5698 188 176 The Sherkaly area has a very poor silicoflagellate complex in which D. frenguellii var. carentis Gleser f. carentis predominates slightly over other forms. Beside the above-mentioned forms, isolated specimens of Distephan- us speculum (Ehr.) Hack. were encountered in the northern part of the West Siberian plain. A detailed comparison of our results with those of Rubina (Rudkevich, Rubina and Permyakov, 1957) and Galerkina (1957) in the West Siberian piain is impossible because many species were defined differently by the various authors. All the silicoflagellate species of the Middle (?) Eocene of the West Siberian plain and the eastern slope of the Urals are also known from the Early Eocene of Western Europe and the Volga area. The Middle (?) Eocene flora of the eastern slope of the Urals and the West Siberian plain differs substantially from the Early Eocene flora of the eastern slope of the Urals. A few typical Early Eocene forms still occur in the Middle (?) Eocene; of these only Dictyocha lamellifera Gleser var. lamellifera is common, while numbers of other forms (D. navi- cula Ehr., D. elongata Gleser, Naviculopsis robusta Defl.) are sharply curtailed. New forms appear, such as the relatively Widespread Dittyocha frenguellilt var. carentis f. carentis Gleser and D. elata Gleser var. elata; these silicoflagellates are occasionally quite numerous. Finally, varieties of Naviculopsis biapiculata (Lemm.) Freng. become more frequent and numerous than in the Early Eocene. The following forms can be regarded as typical of the Middle (?) Eocene flora of the eastern slope of the Urals and the West Siberian plain (Figure 7): Dietyorcita, frenguellii var. carentis Gleser ih ©arentiis Deitametliizera Gieservar. tamerrifera D elata Gleserivar. elata Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata N. b. var. minor (Schulz) Gleser. Silicoflagellates of the Late Eocene A Late Eocene silicoflagellate flora was discovered in many localities in the northern part of the West Siberian plain in the Taz peninsula (the basins of the Arka-Tab-Yakha, En-Yakha, Srednaya Khadyta) and the basin of the Pechal'-Ky (a right tributary of the Taz), as well as on the eastern slope of the Northern and Central Urals (Ivdel' and Serov areas, Ust'- Uiskoe village), the area of the Western Urals (Sherkaly area) and the Middle Ob area. The results obtained are shown in Table 53. Of the 25 species, varieties and forms belonging to 4 genera of the family Dictyochaceae Lemm., the vast majority (20) are of Dictyocha Ehr., many of which are dominant. Naviculopsis Freng. is repre- sented by one species with 2 varieties, characterized usually by high density. Distephanus Stohr and Cannopilus Hack. are each represented by one very rare species. The presence of Cannopilus Hack. in the Late Eocene is of considerable interest, since the species of this genus were hitherto known from the Neogene only. 189 ide | = 3 1 ss ¥ = ay , Ssh 4 + + + Jggopy vyvas “aeA “uw “ c c J y Gc } c c G i! DjDpuNjOL “IEA BSNOL DJvpUNjzoL *C , a a S. = he = ez, = ze Fore ee ee 8 says pynevu “|g a = G € J J V ae V 4 puafijjawD] “ABA JOSOT) V4af1]JawD] *(T c g = a: y Vi g y G z Taso] vj4aaur "y Sizuaivo “sed “f “| c 9 Z e G Gc Gc Z c Z Sijuadpd “} Tasayy Sijuadvo “wea “f° (4 g = z y z I = i i upjansuad{ “wea “[Joq wpjensuaaf -q — — _— _ I — — — -~ —_ “+ + * gmyog puospjuad “ier *f * € g I J g = = ad - = * pyngif *y vyngaf awa “rym 21NgQIf “T a y = G J = > es l J "Se 2) Uip7a SIRA WOSe|s)ev7074" "7. — € — = a i = = = = Josopy) DJINpodd *y vDjajdqwoo “IeA “Pp “(J pee) Soh ra Set Oe SE ly BR sy cc cote een = 1 oe a | 4 = a = e: Fo ee ee ee gasapy pinulov1g ‘IeA tatpuvjfap vyI0hj01q7 SIOAII IOATY yIznyD aBeTTIA uesnkse,a pue . pale rome wiT1y =] eam ,Leqeied 5 AOIaS epat | tATeW puel Areingqin -,1 jo urseq aul ia Ayeysays jo ays e) satoads jo sutseq w-1eyoad Pole PdIv qO 2IPPIW S[eIN ay Jo adoys usoisey e[nsutued ze L qO 12aM07J uretd uetaqts isaM ayi pur sTeip ay jo adojs uJaIsea JYI JO 2UdD0g J1vT JY2 UI SaIv[TABeTJooTIS Jo uoTINGIIsSIq “EG AIAVL (177) € Gh = oD st wD o = oc for) j=) ‘ou aid -WIeS 190 nn ww IOATY uesnkse, ayi jo utseq Bore gO 2TPPpIW (178) 2 z: ®& z | 3 = “ » Me Bes Bt ooo ce rae Se Game (AUq) Snoianydsimay snjidouung) | = Ss ‘3 = dh a = a ‘+ + wary snuospjuad “eA *s “Gg ig c. = a wa I 2. = — ee * unjniads “1A ‘yoret, (ayy) wnynoeds snuvydajsiq é ¢ ¢ ¢ | e z | 7 BOT ay Se ag oy Tae He oe Gace (zjNYOS) sour “eA DyvjnNIIdv1q “Ay G € y S vy tf ] é G "ttt ts pppynaidnig *Jea “BueTy (wway) vypynaidviq sisdojnaiav Ay Zz | _ Z _ i = if a Iasa]) 4oulwm “jy Slwsaul “JeA “7 “CQ eg = = Zz — I — if if i? e MNWeOnsny! “IEA } if c c — I | i y Z[NYIG 4oulw *} vpvjNIIdv “eA *} “CT Xs = . 1 = at ei = a ge CR ORR ia re ae) -noidp *} "WUO'T vypjynoidv “IeA “7 "GT | e “s ° =: I ou EY = So eee ee 8 pygunaniay ‘J DYyjUvIDIA] “JRA “IU DYJUvIVIA? “CG G = a G if G G = = a Se Pe Mao newta2, Oy ae — a JT es == =, == hee a ° = " * * JaseTy (‘TJaq) vsouids ‘gq SIOATI yIzZnyo aBeTTIA pure sous slaqeied ak -,189 ay sotoads jo sutseq s[eIN ay Jo adoys ussisegq pnsutued zey qO 12a Mo0'T N N Ly 9} Gt Vai ‘ou atd -UWIeS (penutiuod) g¢ aTaV.L 191 179 Dictyocha frenguellii var. carentis f. carentis Gleser and f. incerta Gleser, D. rotundata Jousé var. rotundata and Navi- culopsis biapiculata (Lemm.) Freng. var. biapiculata and var. minor (Schulz) Gleser are the most widespread forms. All these silico- flagellates are usually abundant and dominant in the Late Eocene silico- flagellate complexes. Less widespread are Dictyocha deflandrei var. completa Gleser‘f. completa, D. fibula*var. fibula f. fibuta, Do ifen- guelliilbemt var. ireneuellii, D. lamellifera Gleser var. lamellifera, D. transitoria Defl. and the varieties of D. tria- cantha Ehr. Such forms as D. deflandrei var. bicornuta Gleser, D. fibula var. pentagona Schulz, D. navicula Ehr., D. spinosa (Defl.) Gleser and Distephanus speculum (Ehr.) Hack. var. speculum and var. pentagonus Lemm. and Cannopilus hemisphaericus (Ehr.) Hack. are found as isolated specimens in a few localities only. The Late Eocene flora of the investigated parts of the eastern slope of the Urals resembles that of the West Siberian plain. All the areas show a more or less identical species composition and quantitative proportions of the forms, although some differences are evident. For example, Dic- tyocha triacantha var. apiculata f. minor Schulz and Navi- culopsis biapiculata var. minor (Schulz) Gleser predominate in the complex of the Arka-Tab-Yakha River. In the basin of the En-Yakha River Dictyocha frenguellii.var..carentis Gleserd.-caren sa and f. incerta Gleser and D. rotundata Jousé var. rotundata dominate, while in the complex of the Srednaya Khadyta River only the latter two forms dominate. In addition to D. frenguellii var. carentis Gleser f. carentis andf. incerta Gleser and D. rotundata Jousé var. rotundata, the floraofthe Pechal'-Ky Riverisrichin D. transi- toria Defl. and contains considerable amounts of the varieties of Navi- culopsis biapiculata (Lemm.) Freng. The most abundant forms in the Sherkaly area are Dictyocha frenguellii var. carentis Gleser f. carentis andf. incerta Gleser and Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata; here occur isolated specimens of Cannopilus hemisphaericus (Ehr.) Hack., a species rare for the Paleogene. The silicoflagellate flora of the Ivdel' area contains large amounts of many forms: Dictyocha deflandrei var. completa Glese# f. completa, *D.*fibuta Ebr. var. fibela ft. fibula wae the varieties and forms of D. frenguellii Defl., D. rotundata Jousé Var-rotundata. D> transitorivasber.. Dat riacan tina var, apiculata f. minor Schulz and the varieties of Naviculopsis biapiculata (Lemm.) Freng. As in the Sherkaly area, here occur rare specimens of Cannopilus hemisphaericus (Ehr.) Hack. Dictyocha spinosa (Defl.) Gleser is known to be present only in the Ivdel' area. Skeletons of D. lamellifera Gleser var. lamellifera are frequent in the Serov area and rare elsewhere. Only one form — Naviculopsis biapiculata var. minor (Schulz) Gleser — is abundant in the area of Ust'-Uiskoe village. The complex found in the Middle Ob area contains a considerable number of silicoflagellate forms, often in large amounts. Dictyocha frenguellii Defl. var. frenguellii and var. carentis Gleser f. carentis are more abundant here than in other areas; more- over, isolated skeletons are found here of D. navicula Ehr. and 192 Distephanus speculum var. pentagonus Lemm., which were not found elsewhere. A survey of publications on the Late Eocene silicoflagellates of different parts of Western Siberia shows that the different authors agree as to the general nature of the flora. Dictyocha fibula Ehr.s.1l. and Naviculopsis biapiculata (Lemm.) Freng. predominate on the eastern slope of the Northern and Central Urals and in the Trans-Urals (Krotov, 1957a, b; Krotov and Shibkova, 1961) and in the northern part of the West Siberian plain (Radkevich, Rubina and Permyakov, 1957; Galerkina, 1959; Strel'nikova, 1960). Some authors (Strel'nikova, 1. c.) note the occurrence in the areas studied of smaller amounts of Dictyocha transitoria Defl. and the varieties of D. triacantha Ehr., and isolated skeletons of Cannopilus hemisphaericus (Ehr.) Hack. In view of the fact that the above authors place all the forms witha quadrangular basal ring in Dictyocha fibula Ehr. and considering our own observations, it can be stated that the different parts of the West Siberian plain possess an identical Late Eocene silicoflagellate flora. The characteristic silicoflagellate complex of the Late Eocene of the West Siberian plain and the eastern slope of the Urals consists of the following species, varieties and forms (Figure 8): Dietyocha triacantha Ehr. var. triacantha f. triacantha D. frenguel li, Dell. -var..firenguellii D. f. var? Carentrs "Gleserft.carentis Bf. var. Cage nira 4, incerta, Gleser D. deflandrei var. completa Gleserf. completa D. fibula Ehr. var. fibula f. fibula D. rotundata Jousé var. rotundata Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata N. b. var. minor (Schulz) Gleser. The Late Eocene flora of Western Siberia and the eastern slope of the Urals is closely related phylogenetically to the more ancient Middle (?) Eocene flora of the same areas. Through the gradual increase of quali- tative diversity and quantitative development of some species, the Middle (?) Eocene flora merged into that of the Late Eocene. All the Middle (?) Eocene elements persist during the Late Eocene. Most of them become even more abundant except for Dictyocha elata Gleser var. elata and D.lamellifera Gleser var. lamellifera, whose numbers decline. Among Late Eocene forms unknown from the Middle (?) Eocene are D. frenguellii var. carentis f. incerta Gleser, D. deflandrei var. completa Gleserf. completa and vir. pieorniuta Gleser; YD! tibula Ehr.-var: fibula f. fibula. D. transitoria Defl., D. rotundata Jousé, D. spinosa (Defl.) Gleser and species of Distephanus Stohr and Cannopilus Hack. Almost all the above forms are known from the Early Eocene of Western Europe or from the Volga area. New elements appearing for the first time in the Late Eocene are Dictyocha rotundata Jousé, D. spinosa Defl.) Gleser and Cannopilus hemisphaericus (Ehr.) Hack. The last 2 forms (especially D. spinosa) are very rare in the Late Eocene of Western Siberia. 180 193 181 FIGURE 8. Characteristic silicoflagellate complex of the Late Eocene of the eastern slope of the Santonian-Campanian: 1—Dictyocha frenguellii Defl. var. frenguellii; 2, 3—D. f. var. carentis Gleser f. carentis; 4,6—D. f. var. carentis f. incerta Gleser; 5—D. deflandrei var, completa Gleser f. completa; 7—Naviculopsis biapiculata (Lemm.) Freng, var. biapiculata; 8—N.b, var. minor (Schulz) Gleser; 9—Dictyocha fibula Ehr. var. fibula f. fibula; 10—D.triacantha Ebr, var. triacantha f. triacantha; 11, 12— D. rotundata Jousé var, rotundata. For comparison, the Late Eocene flora of the Turgai Gates (Tumalykol' village; Uzen'-Kairakty River) was examined. The Late Eocene flora of Tumalykol' village is comparatively poor (Table 54). It consists of 8 species belonging to the family Dictyochaceae Lemm. Most of these species (5) belong to the genus Dictyocha Enhr.; Distephanus Stohr, Naviculopsis Freng. and Mesocena Ehr. emend. Defl. are represented by one species each. The only characteristic elements of the Middle — Late Eocene of the West Siberian plain and the eastern slope of the Urals present here are Dictyocha rotundata Jousé var. rotundata and Naviculopsis biapiculata var. minor (Schulz) Gleser, which play a minor role in the complex. Dominant here are Distephanus antiquus Gleser and 2 forms of Dictyocha elata Gleser, which are unknown from the Late Eocene of Western Siberia. We have encountered such a flora only in the northern part of the West Siberian plain. The complex of Tumalykol' village will be discussed later in the description of the Early (?) Oligocene silicoflagellates of the West Siberian plain. The Late Eocene flora of Uzen'-Kairakty River, a right tributary of the Irgiz River, has a quite different nature. Here were determined 19 species, varieties and forms belonging to 4 silicoflagellate genera (Dictyocha 194 Ehr., Naviculopsis Freng., Distephanus Stohr and Mesocena Ehr.), all of the family Dictyochaceae Lemm. (Table 54). More than half of the forms belong to Dictyocha Ehr., many of which (D. fibula Ehr. var. fibula fv fiabtla, D. aff. fibula var. rhombus (Hack.) Lemm., and D. spinosa (Defl.) Gleser) are characterized by a considerable density. Distephanus crux (Ehr.) Hack. var. crux dominates the complex. All the remaining forms are not numerous. 182 (181) TABLE 54, Distribution of silicoflagellates in the Late Eocene of northwestern Kazakhstan Tumalykol' |Uzen'-Kairakty ee —— village River 1 | Dictyocha elata var. media Gleser f. media 2 |D.e. var. media f. reducta Gleser . . . _ 3 | D. fibula Ehr. var. fibula f. fibula 4 4 |D. f. var. fibula f. rhombica Schulz 1 5 | D. aff. fibula var. rhombus (Hack.) Lemm. 4 6 |D. hezacantha Schulz 1 7 |D. rotundata Jousé var. rotundata . 1 8 |D. r. var. secta Gleser — 9 |D. spinosa (Defl.) Gleser 4 10 |D. transitoria Def] 1 14 D. triacantha Ehr. var. triacantha f. triacantha 5 aoa ; 2 12 |D. triacantha var. flexuosa (Stradner) Gleser . 2 13 | D. t. var. apiculata Lemm. f. apiculata 3 14 |D. t. var. apiculata f. minor Schulz = 15 | D. t. var. hastata Lemm 1 16 |D. t. var. inermis f. minor Gleser . 17 | Naviculopsis biapiculata (Lemm.) Freng. var. biapiculata 18 | N. 6. var. constricta (Schulz) Gleser . . 19 | N. 6. var. minor (Schulz) Gleser 20 | Distephanus antiquus Gleser . 21 |D. crux (Ehr.) Hack. var. cruz Boke 22 | D. speculum var. cannopiloides (Pr.—Lavr.) Gleser . 23 | D. s. var. pentagonus Lemm. 24 | Mesocena elliptica Ehr. emend. Defl. . 25 | M. aff. apiculata (Schulz) Defl. . . . 26 | M. oamaruensis Schulz 2 oe we | me | we The following small group of forms occurs both in this and in the Late Eocene flora of the eastern slope of the Urals and the West Siberian plain: Dictyocha rotundatia Jouse var. rotundata, D: transitoria Defl., D. triacantha var. hastata Lemm., Naviculopsis bi- apiculata var. minor (Schulz) Gleser. These silicoflagellates, however, are found in rather insignificant numbers in the Uzen'-Kairakty area. Many widespread and abundant characteristic forms of the Late Eocene flora of the Urals and Siberia are not encountered here. A signi- ficant difference of the Turgai flora is the domination of Dictyocha aff. fibula var. rhombus (Hack.) Lemm. and Distephanus crux (Ehr.) Hack. var. crux, and the invariable presence, although in small amounts, of Dictyocha triacantha var. flexuosa (Stradner) Gleser. Figure 9 shows the characteristic silicoflagellate complex of the Uzen'- Kairakty River. 195 FIGURE 9. Characteristic silicoflagellate complex of the Late Eocene of the Uzen'-Kairakty River, a tributary of the Irgiz River: 1—Distephanus speculum var. pentagonus Lemm.; 2, 3—D. crux (Ehr.) Hack. var. crux; 4—Dictyocha fibula Ehr. var. fibula f. fibula; 5—D. aff. fibula var. rhombus Schulz; 6—D. triacantha var. apiculata Lemm. f. apiculata; 7—D.t. var. flexuosa (Stradner) Gleser; 8—D. spinosa (Defl.) Gleser. Analysis of original materials and published data shows that the Late Eocene silicoflagellate flora differs from one part of the globe to another. While species of Dictyocha Ehr. and Naviculopsis Freng. attain considerable density in the West Siberian plain and on the eastern slope of the Urals, the flora of the Turgai Gates is dominated by representatives of Dictyocha Ehr. and Distephanus Stohr, and Naviculopsis Freng. and Distephanus Stohr are the most typical forms of the Californian flora. Of species common in the Late Eocene to all regions, Naviculopsis biapiculata (Lemm.) Freng. must be noted. This species is known from Western Siberia and Kazakhstan, as well as from southern Sweden (Cleve-Euler and Hessland, 1948) and California (Hanna, 1931; Clark and Campbell, 1945; Mandra, 1960). As in Western Siberia, this species is represented in California by 2 varieties which occur in large numbers (Mandra, 1960). Varieties of Dictyocha triacantha Ehr. are also shared with the Californian flora. One form, D. deflandrei var. completa Gleserf. completa (D. staurodon Ehr. as deter- mined by Cleve-Euler, l.c.), has been encountered in Sweden and Western Siberia. 183 196 Silicoflagellates of the Late Eocene — Early Oligocene (?) Results of the investigation of the silicoflagellate flora of the Late Eocene — Early Oligocene (?) in the southern part of Taz peninsula (the basins of the Srednaya Khadyta and the En-Yakha), in the basin of the Malaya Sosva, in the Ivdel' area on the eastern slope of the Northern Urals and in the Middle Ob area are given in Table 55. (185) TABLE 55. Distribution of silicoflagellates in the Late Eocene — Early Oligocene (?) of the eastern slope of the Urals and the West Siberian plain Taz peninsula No. Species pests Lower Ob area, Malyi Atlym Basin of the Severnaya Sosva and Malaya Sosva rivers Eastern slope of the Urals, Ivdel' area En-Yakha River (right bank) Srednaya Khadyta and Chuzik rivers 1 Dictyocha deflandrei var. bi- cornuta Gleser. . . 3 _ -- 2 5 4 2 2 D. d. var. completa Gleser f. completa .. 1 1 1 2 4 5) 3 3 WD de VaE: completa f. producta Gleser . . a3 4 _ 2 3 3 4 ) 4 3 elata Gleser var. elata... 1 -- _ — — = — 5 fibula Ehr. var. fibula f. gat : PI. 4 — 3 4 5) 5 5) 6 Drei-var: fibula f. “rhombica SUCOULZ 5s ens ee te Be — _— _— = 1 a= = if aes Nar: pentagona Schulz | — a _ os — 1 — 8 D. frenguellii Defl. var. — guellii . 1 = — 1 1 = = 9 DB: re var. carentis Gleser f. ca- rentis . : 3 1 1 3 5 4 3 10 De feo wars carentis f. incerta Gleser . . seis iste Hes 2 2 1 4 5 4 1 14 D. obliqua Gleser. : -- — — 2 3 — — 12 D. rotundata Jousé var. rotun- data Ken cape 6 5 D 6 4 4 4) 13 D. r. var. secta Gleser . . . 5 3 3 3 — 4 4 14 D. spinosa (Defl.) Gleser . 1 — — 1 4 _ 1 15 D. transitoria Def). : 3 3 4 3 3 4 3 16 D. triacantha Ehr. var. tria- cantha f. triacantha. . . . — — — = — — 4 17 D. t. Ehr. var. gies mi- nor Schulz. . . . -| — — — _ 1 = 18 D. t. var. hastata Lemm. . .| — - 1 _ = 1 F 19 D. t. var. inermis f{. minor Gléser oP Let et ES — _ — _ 1 = 20 Naviculopsis biapiculata (Lemm.) prone var. biapi- ; culata . 3 = 3 3 4 a 2 21 N. b. var. minor (Schulz). Gle- Sere: 5 1 3 5 5 5 =) 22 Distephanus ‘speculum (Ehr.) Hack. var. speculum. ...| — — — -- — = 1 23 D. s. var. pentagonus Lemm. | — — — ~ = L az 24 Cannopilus gry aplenty Gem,» RAS) = 1 — — a = = 25 Mesocena circulus are bie = = 1 1 = — 197 184 The silicoflagellate flora of these stages numbers 25 species, varieties and forms belonging to 5 genera of the family Dictyochaceae Lemm. Most (19) of the silicoflagellate species, varieties and forms belong to the genus Dictyocha Ehr., while other genera are represented by one species each. Wide distribution and high numerical development charac- terize D. rotundata Jousé var. rotundata and Naviculopsis biapiculata var. minor (Schulz) Gleser. Other forms occurring in almost all of the areas examined but in smaller numbers are Dictyocha deflandrei var..bicornuta Gleser and var. completa Gleser f. completa andf. producta Gleser,. D..fibuda,Ehr., var. fibuda = fibula, D.frenguellii'var. car entis,Cieser.tf. .carentis-ame & incertaGleser: Derotundata var: secta Gleser,-Drtransi ror Defl. and Naviculopsis biapiculata (Lemm.) Freng. var. biapi- culata. D.elata Gleser var. elata, D. obliqua Gleser, D. spinosa (Defl.) Gleser, varieties of D. triacantha Ehr. and Distephanus speculum (Ehr.) Hack., Cannopilus hemisphaericus (Ehr.) Hack., Mesocena circulus Ehr., ete. occur as very rare or rare, but D. obliqua Gleser appears once as frequent. The complex of the southern part of the Taz peninsula and the Middle Ob area are almost identical, except for some variations in the density of certain forms. The flora of the basin of the Malaya Sosva altogether resembles that of the Taz peninsula, although it contains rare specimens of D. obliqua Gleser, not found in the latter area. Special features of the silicoflagellate complex of the Ivdel' area are the complete absence of D. rotundata var. secta Gleser, the lower density of D. rotundata var. rotundata compared to other areas, and the relatively greater amounts of D: deflandrei-var.-bicornuta Gleser’D.frengweiine var. carentis Gleser f. caréentis andf. incerta. Gleser. The characteristic complex of the Late Eocene — Early Oligocene (?) of the eastern slope of the Urals and the West Siberian plain consists of the following silicoflagellates (Figure 10): Dictyocha deflandrei var. completa Gleserf. completa Dp. d.iwar-.s Bae 2 D. elata var. media Gleser f. media 5 4 3 D. e. var. media f. reducta Gleser . . . 6 5 5 4 D. fibula Ehr. var. fibula f. fibula : -- 1 5 D. frenguellii var. carentis Gleser f. ca- TERS: 2 TAB ad oy 4 RR EEK 3 J { 6 D. f. var. carentis f. incerta Gleser 1 : 1 7 iD: oolgna Glaser =. (0 sop. ee -- 1 —_ 8 D. spinosa (Defli) Gleser)i.c2 2. . = . 4 3 — 9 D. rotundata Jousé var. rotundata . 4 3 3 10 Dr: Mare SeChe MaleSEL Vote els oe ws 3 4 1 11 De transite mice OI el ooo pe Souci anys anys 2 2 1 12 D. triacantha var. apiculata f{. minor Schulzteremete te ete owe seas 2 it — — 13 iD. tavar: hastaba Piemm sone. yt _ 1 — 14 D. t. var. inermis {. minor Gleser . .. . — 1 1 15 Naviculopsis biapiculata (Lemm.) Freng. Van.. biapiculata® 2) ah 8 oe 1 — — 16 N. b. var. minor (Schulz) Gleser — 4 2 17 Distephanus antiquus Gleser. .... . 5 5 5 18 D. speculum var. pentagonus Lemm. . . — 1 a 19 Mesocena elliptica Ehr. emend. Delf. . . 1 3 2 The majority (14) of these forms belong to the genus Dictyocha Ehr.; the genera Naviculopsis Freng. and Distephanus Stohr are repre- sented by 2 forms each, and Mesocena Ehr. by one form. Dictyocha elata var. media Gleserf. media andf. reducta Gleser and Distephanus antiquus Gleser are the most abundant forms everywhere. Equally ubiquitous but less numerous are Dictyocha ASt ede ells var. carentis Gleserf. carentis and f. incerta 200 Gleser, varieties of D. rotundata Jousé, D. transitoria Defl., Mesocena elliptica Ehr. emend. Defl. D. spinosa Defl. and Naviculopsis biapiculata occur in considerable amounts, but show a more limited distribution. Among the rare forms here are Dictyocha deflandrei var. completa Gleserf. completa, D. fibula Ehr. var. fibula f. fibula, D. obliqua Gleser, varieties of D. triacantha Ehr. and Distephanus speculum var. penta- gonus Lemm. Nearly all forms in the southern part of the Taz peninsula show a greater density than those in the basin of the Pelym River. This may be due partly to the larger amount of material examined from the former area. = 9 14 FIGURE 11. Characteristic silicoflagellate complex of the Early Oligocene (?) of the West Siberian plain; 1,3—Dictyocha elata var. media Gleser f. media; 2—D. e. var. media f. reducta Gleser; 4,5—Distephanus antiquus Gleser; 6—Dictyocha spinosa (Defl.) Gleser; 7,9—Mesocena elliptica Ehr. emend. Def.; 8, 10—Dictyocha rotundata Jousé var. rotundata; 11-13, 15—D. +r. var. secta Gleser; 14—Naviculopsis biapiculata var. minor (Schulz) Gleser. The characteristic silicoflagellate complex of the Early Oligocene (?) of the West Siberian plain consists of the following species, varieties and forms (Figure 11): Dictyocha elata var. media Gleserf. media DD. evwaro media fered uctaGleser D. rotundata Jousé var. rotundata Dor. vars pec tavGleser D. spinosa (Defl.) Gleser Naviculopsis biapiculata var. minor (Schulz) Gleser Distephanus antiquus Gleser Mesocena elliptica Ehr. emend. Defl. 201 188 189 190 The Early Oligocene (?) silicoflagellate flora of the southern part of the Taz peninsula differs from that of the Late Eocene — Early Oligocene (?) in the predomination of forms either unknown in the earlier stage of Western Siberia (Dictyocha elata var. media Gleser f. media and f. reducta Gleserand Distephanus antiquus Gleser)orvery rarethere (Dictyocha spinosa (Defl.) Gleser). The transition between the floras is evident in the presence of forms typical of both stages, such as the varieties of Dictyocha rotundata Jousé and Naviculopsis biapiculata var. minor (Schulz) Gleser. There are more small, rounded forms in the Early Oligocene (?) than in the Late Eocene — Early Oligocene (?). A similar flora, which we encountered in the Tas-Aran suite of the northern Aral area, is dated in the Late Eocene. This discrepancy in the dating of two such closely related complexes seems to be due to inaccurate dating of one of them. Recently, there has been a tendency to regard the rocks of the lower part of the Chegan suite containing remains of siliceous organisms (radiolarians, diatoms and dinoflagellates) as part of the Lyulimvor suite. According to the unified stratigraphic scheme (Uni- fitsirovannaya regional'naya..., etc., 1961), the upper part of the Lyulimvor suite belongs to the lower half of the Late Eocene. Thus, the discussed silicoflagellate flora cannot be dated as Early Oligocene (?), but at the beginning of the Late Eocene. Such a determination is much closer to the analogous flora or the northern Aral area. However, this assumption must be verified by a thorough study of the latter silicoflagellate flora. We date tentatively in the Early Oligocene the silicoflagellate flora of the Kharkov suite of the European USSR. Very little has been published on the silicoflagellates of the Kharkov suite. Uspenskaya (1950) notes that the microfloral and microfaunal associations of the Kharkov stage of the city of Kharkov contain Dictyocha fibula Ehr., D.triommata Ehr. (]D. trigeantha Ehed; Dercerax Ehr. (= Distephanus crms (Ehr.) Hack.) and D. speculum Ehr. (=Distephanus speculum (Ehr.) Hack.), while the association of Verino Pole village contains only one species — D. fibula Ehr. Silicoflagellate fossils were encountered in the Kharkov suite at the following localities: the basin of Oskol River (Krasnyi Oskol village), in the Sumy Region (Boromlya village), on the left bank of the Dnieper near Dnepropetrovsk and in the Kharkov Region (in the villages of Staroverovka and Melovoe) (Table 57). Figure 12 shows the characteristic silicoflagellate complex of the Early Oligocene (?) of the Ukrainian SSR. A total of 16 silicoflagellate species, varieties and forms belonging to 5 genera (Dictyocha Ehr., Naviculopsis Freng., Distephanus Stohr, Cannopilus Hack. and Mesocena Ehr.) of the family Dictyo- chaceae Lemm. were determined. Most of these belong to the genus Dictyocha Ehr.; the genus Naviculopsis Freng. is represented by one species with 2 varieties, Mesocena Ehr. and Distephanus Stohr by 2 species each, and Cannopilus Hack. by one species. Almost all the forms occur at a low density. The predominant elements are Dictyocha spinosa (Defl.) Gleser, D. hexacantha Schulz, Distephanus crux (Ehr.) Hack. var. crux and Naviculopsis biapiculata var. minor (Schulz) Gleser. Except for the new species Mesocena muticata Gleser, all these silicoflagellates are also known 202 from the Paleogene of other parts of the globe. Of particular interest is the presence of Dictyocha hexacantha Schulz, D. spinosa (Defl.) Gleser and D. triacantha var. flexuosa (Stradner) Gleser. The first is known from the Late Eocene of the basin of the Irgiz River and from the Late Eocene or Late Eocene — Early Oligocene of Oamaru (New Zealand) and California. Considerable amounts of skeletons of D. spinosa (Defl.) Gleser were found by us in the Lower Oligocene (?) deposits of the southern partof the Taz peninsula. Inaddition, this silicoflagellate has been reported from the Late Eocene— Early Miocene deposits of Barbados Island (Lesser Antilles). The latter form is known from the Late Eocene of the basin of the Irgiz River, the Late Oligocene of the Mangyshlak peninsula and Austria. (188) \ eS pas ie FIGURE 12. Characteristic silicoflagellate complex of the Early Oligocene (?) of the Ukrainian SSR; 1 —Dictyocha fibula Ehr. var. fibula f. fibula; 2-Mesocena oamaruemnsis Schulz var. oamaruensis; 3—Dictyocha hexacantha Schulz; 4—D. spinosa (Defl.) Gleser; 5—D.triacantha Ehr, var, tria- cantha f, triacantha; 6—Naviculopsis biapiculata var, minor (Schulz) Gleser; 7—-Mesocena muticata Gleser; 8—Dictyocha tria- cantha var. flexuosa (Stradner) Gleser; 9—Distephanus crux (Ehr.) Hack. var. crux. 203 (189) TABLE 57. Distribution of silicoflagellates in the Early Oligocene (?) of the Ukrainian SSR Dnepro- Kharkov Region petrovsk Region left bank of No. Species E : Dnieper Staro- Krasnyi Boromlya | Melovoe River near ‘ . verovka Oskol ; village village . ; Nizhne- village village A. Dneprovskii Uzel station 1 | Dictyocha bimucronata (Defl.) Tsumura .... — _ 1 — -— 2 |D. fibula Ehr. var. fibula gt SH) Ree aie = u's a 1 1 3 |D. f. var. fibula f. rhombica Schnee ee es os - -- 1 _ _ 4 |D. hexacantha Schulz .. . — — 1 — 3 5 | D. spinosa (Defl.) Gleser = = 4 2 1 6 |D. rotundata Jousé var. ro- TUTE QUAE Seo eh i) sae — _ — — 7 |D. r. var. secta Gleser . . — = | = -- 8 | D. triacantha Ehr. var. tria- cantha f. triacantha. . . —_ — 1 — 1 9 |D. t. var. flexuosa (Strad- ner) wWaleser*. Var. & _ = 1 1 1 10 | Naviculopsis biapiculata (Lemm.) Freng. var. bia- PiCularagre <5 bee Se, be _ -- -- - 1 11. | N. b. var. minor (Schulz) Glaser. <2 5) 1 ae _ 3 3 1 12 | Distephanus cruz (Ehr.) 1 Hack.) vari crime Sigse 1 — 3 1 1 13. |D. speculum (Ehr.) Hack. Var. “Spemuuntaes . ts . oo — 1 — _— 14 | Cannopilus hemisphaericus (Ebr) Hack Va 3. on - oe — _ 1 15 | Mesocena muticata Gleser _ -- 1 _ 1 16 | M. oamaruensis Schulz . . _ - 1 There is at present no reliable information on the silicoflagellate flora’ of the Early Oligocene. Silicoflagellates of the Late Oligocene Late Oligocene silicoflagellates are known from Austria (Stradner, 1961). Remains of a Late Oligocene silicoflagellate flora have also been found inthe diatomites of the Karagan suite of the Mangyshlak peninsula. Here the flora is fairly uniform; altogether 4 forms have been determined (Figure 13). One of these belongs to the genus Dictyocha Ehr., two to Distephanus Stohr, and one toMesocena Ehr. Mesocena elliptica Ehr. is very abundant; Distephanus speculum (Ehr.) Hack. var. speculum is abundant; D. crux (Ehr.) Hack. var. crux and Dictyocha triacantha var. flexuosa (Stradner) Gleser are frequent. Skeletons of Mesocena elliptica Ehr. show a great variety. Distephanus speculum (Ehr.) Hack. var. speculum 204 191 is represented by 2 forms, one of which is numerous and has slightly elongated skeletons with 2 very long radial horns (Figure 13, 3), whereas the other form is rare. D. crux (Ehr.) Hack. var. crux is distinguished by its very small size. Except for Distephanus speculum (Ehr.) Hack. var. speculum, all the forms found in Mangyshlak are common to the Late Oligocene silicoflagellate complex of Austria. (191) 5 FIGURE 13. Characteristic silicoflagellate complex of the Late Oligocene of Mangyshlak peninsula; 1—Dictyocha triacantha var. flexuosa (Stradner) Gleser; 2—Distephanus crux (Ehr.) Hack. var. crux; 3,4—D. speculum (Ehr.) Hack. var. speculum; 5—Mesocena elliptica Ehr. emend. Defl. The material examined shows that the family Dictyochaceae Lemm. proliferated during the Paleogene. Some members of Vallacertaceae Defl., a family typical of the Cretaceous, disappear completely already at the beginning of the Paleocene. The Paleocene is characterized by the proliferation mainly of one species — Dictyocha triacantha Ehr.— which appeared in the Cretaceous but at no appreciable density. The number of species of Dictyocha Ehr. increases sharply during the Early Eocene, when two new genera, Distephanus Stohr and Navi- culopsis Freng., appear. One species of the latter, N. biapiculata (Lemm.) Freng., was widespread all over the globe during the Eocene (according to certain data also during the Early Oligocene). In the Middle and Late Eocene several species of the Dictyocha Ehr. appeared, and many of the Paleocene and Early Eocene species of this genus continued to 205 192 flourish. Several new species of Distephanus Stohr appeared during the Late Eocene. At the same time a new genus Cannopilus Hack. emerged, whose occurrence is very rare. While the floras of the Paleo- cene and the beginning of the Early Eocene differ little from one area to another, there are marked differences between the known Late Eocene complexes of Western Siberia, Kazakhstan (Irgiz Basin, northern Aral area) and California. These differences could be clarified either by a more accurate dating of the Eocene complexes of the eastern slope of the Urals and the West Siberian plain or by a thorough study of the composition and changes in the silicoflagellate complexes outside the confines of Western Siberia. Silicoflagellates of the Neogene Silicoflagellates are known from the Neogene of many parts of Europe, North Africa, Asia, and North and South America. The silicoflagellates of the area of Mor6én in Spain were investi- gated in a number of taxonomical studies (Lemmermann, 1901b; Schulz, 1928; Gemeinhardt, 1930; Deflandre, 1932a, b, 1950; Frenguelli, 1940). A list of forms encountered is to be found only in the article by Deflandre (1932a), but quantitative data, as in the other publications, are absent. In a study of the silicoflagellate flora and its stratigraphic position, Colom (1952) notes that in Spain, silicoflagellate skeletons and diatom frustules occur in deposits named moronitas; in the area of the North Betic Strait, these deposits belong to the Aquitanian-Burdigalian stage of the Late Oligocene or Early Miocene. Among the silicoflagellates Dictyocha fibula Ehr. and its varieties are most abundant, and species of Mesocena Ehr. (M. elliptica Ehr. emend. Defl.) are numerous. On the other hand, Distephanus Stohr is encountered rarely, and D. speculum (Ehr.) Hack. is encoun- tered in larger amounts only in the Andalusian zone where the cold waters of the Atlantic Ocean penetrated. Further information on the silico- flagellates of Spain can be found in the earlier works of Colom (1940, 1946). The Neogene silicoflagellates of Italy were studied by several workers (Ehrenberg, 1854; Lemmermann, 1901b; Cocco, 1904—1905; Carnevale, 1908; Schulz, 1928; Gemeinhardt, 1930; Deflandre, 1950, andothers); almost all of these authors used the Italian material for working out the system- atics of the group. According to the literature, the Neogene flora of Italy consists mainly of species of Dictyocha Ehr..and Distephanus Stohr. Dictyocha ausoOnia Defl. has been reported from many parts of Italy (Deflandre, 1950). From the Tortonian facies of the Middle Miocene of Grotte, Sicily, Deflandre established the new genus Nothyocha Defl. with a single species, N. insolita Defl., unknown from any other locality. The silico- flagellates of Italy are discussed in the major work of Zanon (1934). No special works have been published on the silicoflagellate flora of Greece. From the studies of Ehrenberg (1841, 1854), Lemmermann (1901b), Schulz (1928), Gemeinhardt (1930) and others it appears that the dominant species of the Neogene of Greece is Mesocena elliptica Ehr. emend. 206 193 Defl.; also known from there are varieties of Distephanus crux (Ehr.) Hack. and D. speculum (Ehr.) Hack., Paradictyocha poly- actis Freng. and one species of Dictyocha Ehr. — D. navicula Ehr., unknown in the Neogene of other areas. In the Sarmatian of Yugoslavia, Schulz (1928) and Gemeinhardt (1930) encountered varieties of D. fibula Ehr., Distephanus crux (Ehr.) Hack., Naviculopsis biapiculata (Lemm.) Freng., etc. Jerkovic (1965) described several new species and the genus genus Deflandryo- cha Jerk. from this stage. The Miocene of Hungary contains a fairly varied silicoflagellate flora found at a large number of localities (Lemmermann, 1901b; Schulz, 1928; Gemeinhardt, 1932; Deflandre, 1932a, 1950; Frenguelli, 1940). Apparently, a significant morphological variation of skeletons characterizes the cannopiluslike forms of Distephanus speculum (Ehr.) Hack. and Dictyocha macilenta Defl. The latter species is probably a close relative of Distephanus crux (Ehr.) Hack.; Cannopilus sphaeri- cus Gem. is typically present. The Miocene silicoflagellate flora of Oran (North Africa) consists of species widely distributed in the Neogene—D. fibula Ehr., Distephanus crux (Ehr.) Hack., Mesocena elliptica (Ehr.) Defl., etc. (Ehrenberg, 1841, 1854; Schulz, 1928; Gemeinhardt, 1930; Deflandre, 1932a). The Miocene of India (Nankoori) has a similar silicoflagellate flora (Ehrenberg, 1851, 1854; Lemmermann, 1901b; Schulz, 1928; Gemeinhardt, 1930; Desikachary and Macheshwari, 1956). In India (Colebrook), Desikachary and Macheshwari found skeletons of Dictyocha tria- cantha var. triacantha f. minor Schulz. This finding leads them to assume that the Colebrook deposits are older than those of Nankoori, a view which is supported by certain geological data. Most of the major taxonomists have used the Neogene silicoflagellates of Japan for solving various problems of the classification of the group (Schulz, 1928; Gemeinhardt, 1930; Frenguelli, 1940; Deflandre, 1950; Tsumura, 1963). Deflandre described the new species Dictyocha japonica Defl. and D. retrospina Defl. from the Miocene of Honshu Island, and pub- lished a list of the species occurring on Honshu Island (Sendai) (Deflandre, 1932a). The flora of the Late Miocene— Early Pliocene of Noto peninsula and the environs of the city of Kanazawa is listed in the article of Ichikawa (1950). In another publication (Ichikawa, 1956) complexes found in 6 hori- zons of Late Miocene deposits in different areas around Hokuriku (Honshu Island) are described in detail, and a total of 22 silicoflagellate species, varieties and forms were determined, of which the most widespread and abundant is Distephanus crux (Ehr.) Hack. Dictyocha fibula Ehr. , represented by several forms, occurs almost ubiquitously and in considerable amounts. Less widespread are the varieties of Distephan- us speculum (Ehr.) Hack., although in some places their skeletons occur in large numbers. Cannopoloides forms of this species are very rare. Mesocene elliptica (Ehr.) Defl. is often abundant in some places. Dictyocha triacantha Ehr. is abundant in the Toyama area, while Paradictyocha polyactis Freng. f. polyactis is abundant in the Iizuka horizon of the Suzu area. The Neogene silicoflagellates of Japan are described in an important work by Bachmann and Ichikawa (1962). 207 Silicoflagellates are known from many parts of the Neogene of North America (Ehrenberg, 1854; Lemmermann, i901b; Martin, 1904; Schulz, 1928; Hanna, 1928b; Gemeinhardt, 1930; Deflandre, 1932a, b; Frenguelli, 1940; Tynan, 1957; Mandra, 1960). Of particular interest are the articles of Tynan and Mandra. These authors discuss the age and exact stratigraphic position of the silico- flagellates, and present lists and the quantitative relation of forms in the complex. Tynan describes the Middle Miocene silicoflagellate flora of the Calvert formation in Maryland. Distephanus crux (Ehr.) Hack. is dominant here, its skeletons accounting for about 90% of the total; second is D. speculum (Ehr.) Hack. with about 10%, represented by highly variable cannopiloides forms. Mesocena apiculata (Schulz) Defl. contributes about 1%, while Corbisema trigona (Zittel) Defl. (= Dictyocha triacantha Ehr.) is even less frequent. Mandra studied the silicoflagellates of the Middle Miocene, Late Miocene and Miocene — Pliocene of California. He notes that only 4 of the 22 species he determined in the Miocene of California are known from the Eocene of the same region. After a statistical analysis of his results, Mandra concludes that the following 5 species are characteristic of the Miocene of California: Cannopilus calytra Hack. (= Distephanus octonarius var. cyrtoides (Hack.) Gleser), C. hemisphaericus (Ehr.) Hack., Distephanus crux (Ehr.) Haéck., D. speculum var. brevispinus Lemm. (= D. speculum (Ehr.) Hack. var. speculum) and Mesocena crenulata var. diodon (Ehr.) Lemm. (= M.elliptica Ehr. emend. Defl.). The presence of two species — Mesocena crenulata var. diodon (Ehr.) (= M. elliptica Ehr. emend. Defl.) and Cannopilus sphaericus Gem. — characterizes the Mohnian stage (Upper Miocene), whereas the Delmontian stage (Upper Miocene or Miocene — Pliocene) is associated with a single species — Distephanus ornamentum (Ehr.) Hack. (= D. speculum (Ehr.) Hack. var. speculum). The silicoflagellate flora of Barbados Island (Lesser Antilles) has a peculiar composition. Deflandre (1950) places this complex in the Late Oligocene— Early Miocene. In Barbados deposits, Lemmermann (1901b), Schulz (1928), Gemeinhardt (1930) and Deflandre (1950) found Dictyocha staurodon Ehr., D.hexacantha Schulz, Phyllodictyocha recta Defl.,. Corbisema bimucronata Defl., C. spinosa Defl., Navi- culopsis foliacea Defl., Distephanus speculum (Ehr.) Hack., Mesocena elliptiea Ehr: emend. ‘Defl.,-ete: A list of the silicoflagellates of the Neogene of South America (Bolivia) is given in an article by Deflandre (1932a); Frenguelli (1940, 1951) also studied this flora. Few authors have discussed the silicoflagellates of the Miocene of the southern part of the European USSR. Gaponov (1914, 1915) deals with the diatoms and silicoflagellates of the Sarmatian stage of the Khmel'nitskii and Dnepropetrovsk regions, Makarova (1960) with the silicoflagellates of the Sarmatian and Meotian stage of the Taman peninsula, and Kozyrenko (1959) with those of the Sarmatian of Crimea. Present-day and fossil silico- flagellates of the Black Sea basin are reviewed in a work by Proshkina- Lavrenko (1959), which treats the floras of the Sarmatian stage at Shibik in the Krasnodar Territory and of the Sarmatian and Meotian stages of the 194 208 195 Taman peninsula, together with descriptions and drawings of the forms encountered. According to the above authors, this flora contains a moderate amount of species. Gaponov encountered numerous skeletons of Distephanus crux (Ehr.) Hack. var. crux inSarmatian deposits of the Konka River near the town of Orekhovo, Dnepropetrovsk Region, as well as in Kremenno village, Khmel'nitskii Region. In the latter locality he also found sparse remains of Dictyocha fibula Ehr. var. fibula f. fibula and Distephanus speculum (Ehr.) Hack. var. speculum. Inthe Meotian stageof the Tamanpeninsula, Proshkina- Lavrenko found D. crux (Ehr.) Hack. var. crux, Dictyocha fibula Ehr. var. fibula f. fibula, D. navicula Ehr. and Mesocena elliptica Ehr., and noted that the first two species are distinguished by high polymorphism. Makarova (l.c.) determined another species of Distephanus Stdhr in the same materials, D. speculum (Ehr.) Hack. var. speculum with frequent occurrence, and discovered isolated skeletons of Dictyocha triacantha var. triacantha f. minor Schulz in the Sarmatian stage of Cape Panagii in the Taman peninsula. The only silicoflagellate known from the Sarmatian stage ofthe Crimeais Distephanus crux (Ehr.) Hack. var. ©r us. There is little information in the literature on the Neogene silico- flagellates of the Soviet Far East, and no special works have been published; silicoflagellates were studied together with the diatoms. Three forms of the genus Distephanus have been reported from the Neogene of Kamchatka. Gaponov (1927) found considerable amounts of fragments of Distephanus crux (Ehr.) Hack., while Sheshukova- Poretskaya (1961) mentions 3 forms: D. crux (Ehr.) Hack., D. speculum (Ehr.) Hack. and D. speculum var. septenarius (Ehr.) Jorg., all of very rare occurrence. In the rocks of the Kurasi(?) and Maruyama suites of southern Sakhalin, Sheshukova-Poretskaya (1959) encountered the remains of 5 silicoflagellate species. The most abundant and wide- spread is D. speculum (Ehr.) Hack. Only one sample from the Maruyama suite of the Gurovka (Ko-Utori) River contained appreciable amounts of D. crux (Ehr.) Hack. Isolated specimens of Dictyocha fibula Ehr., D. japonica Defl. (=Distephanus japonicus f. pseudofibula (Schulz) Gleser) and Naviculopsis biapiculata (Lemm.) Freng. (forma) occurred in some samples. We studied the Neogene silicoflagellate flora in materials from the Caucasus, Sakhalin, Kamchatka and the Kurile Islands. A total of 18 silicoflagellate species, varieties and forms belonging to 5 genera, all of the family Dictyochaceae Lemm., were found. Most of the species (4) belong to Distephanus Stdhr.; species of this genus are often polymorphic, as indicated by the considerable number of intra- specific forms (9). The genus Dictyocha Ehr. is represented by 3 species with 5 varieties and forms. The genera Cannopilus Hack., Mesocena Ehr. and Paradictyocha Freng. are represented by one species each. Almost all the species of Distephanus occur in considerable amounts. Distephanus crux (Ehr.) Hack. var. crux and D. japonicus f. pseudofibula (Schulz) Gleser are very abundant; D. speculum (Ehr.) Hack. var. speculum and D. speculum var. pentagonus Lemm. are abundant; D. speculum var. cannopiloides (Pr.-Lavr.) Gleser 209 196 is common. Among the remaining species, only Dictyocha fibula Ehr. var. fibula f. fibul@ is numerous. Inthe Early Miocene of the Shibik River (Krasnodar Territory) we found only 2 species — Distephanus crux (Ehr.) Hack. var. crux (very abundant) and Dictyocha triacantha Ehr. var. triacanitha f. triacantha (very rare). This flora resembles that of the Sarmatian and Meotian stages of other parts of the Black Sea area in the abundance of Distep hanas’ crux (Ehr.) Mack: var.) € f ux ; In the Neogene of the Far East, 17 silicoflagellate species, varieties and forms were determined. Of these, 9 belong to the genus Distephanus Stohr, 4to Dictyocha Ehr., 2to Paradictyocha Freng., and one each to Mesocena Ehr. and Cannopilus Hack. (Table 58). TABLE 58. Distribution of silicoflagellates in the Neogene of the Far East Sakhalin Kurile northern Islands part southern (Shmidt part peninsula) Kam- chatka Species 1 | Dictyocha ausonia Defl. ........ _ - 1 — 2 | D. fibula Erh. var. fibula lf. fibula ... 4 _ 5 1 3 |D. f. var. fibula f. rhombica Schulz . . _ -- 1 — 4 |D. f. var. pentagona Schulz...... 1 1 3 — 5 Distephanus crux (Ehr.) Hack. var. cruz 5 — 5 1 6 |D. japonicus (Defl.) Gleser f. japonicus - -- 1 — 7 |D. 7. £ pseudofibula (Schulz) Gleser . . — _- 5 6 8 |D. octonarius (Ehr.) Defl. var. octonarius — _— 4 — 9 |D. o. var. polyactis (Jorg.) Gleser . . . 2 -- 1 _ 10 |D. speculum (Ehr.) Hack. var. speculum 1 5 5 5 11 D. s. var. cannopiloides (Pr.-Lavr.) Gle- 1 Cs ae See a Rae eee. tee 2 4 1 42 D. s. var. pentagonus Lemm. .... . 1 2 5 2 13 D. s. var. septenarius (Ehr.) Jorg... . 1 1 3 — 14 Paradictyocha polyactis Freng. f. polya- CUS Le ee Soe. eke ee ate eS — -— 2 1 15 P. p. f. mesocenoidea Freng. .... . — — 2 1 16 Mesocena stellata Hack. ........ — - { — 17 Cannopilus hemisphaericus (Ehr.) Hack. _ — 1 — The following silicoflagellates are common to Kamchakta, Sakhalin and the Kuriles: Dictyocha fibula var. pentagona Schulz and varieties of Distephanus speculum (Ehr.) Hack. (var. speculum, var. pentagonus Lemm., var. septenarius (Ehr.) Jorg. and var. cannopiloides (Pr.-Lavr.) Gleser). Almost all the forms occurring in Kamchatka and the Kurile Islands are also known from Sakhalin. On the other hand, some of the Sakhalin forms (Dictyocha ausonia Defl., D. fibula var. fibula f. rhombica Schulz, varieties of Distephanus japonicus (Defl.) Gleser, D. octonarius (Ehr.) Defl. var. octa- narius, and Paradictyocha polyactis (Ehr.) Freng., Mesocena stellata Hack. and Cannopilus hemisphaericus (Ehr.) Hack.) were not found in Kamchatka or on the Kurile Islands. In the Far East, an older complex of Neogene silicoflagellates is known from the northern coast of the Shmidt peninsula and in the basin of the Kongi 210 197 and Tumi rivers (Figure 14). Characteristic of this complex is the greater amount of Distephanus crux (Ehr.) Hack. var. crux and D. specu- lum var. cannopiloides (Pr.-Lavr.) Gleser in comparison with the remaining, less numerous Dictyocha fibula Ehr. var. fibula f. fibula, Distephanus speculum (Ehr.) Hack. var. speculum, var. pentagonus Lemm. and var. septenarius (Ehr.) Jorg., D. japonicus f. pseudofibula (Schulz) Gleser, Cannopilus hemi- sphaericus (Ehr.) Hack. and Mesocena stellata Hack. The most abundant form on the northern coast of the Shmidt peninsula is Distephanus crux (Ehr.) Hack. var. crux; D. speculum var. cannopiloides (Pr.-Lavr.) Gleser occupies the second place. In the basin of the Kongi and Tumi rivers this relationship is sometimes reversed. Moreover, D. speculum (Ehr.) Hack. var. speculum appears in slightly larger quantities in the latter locality. FIGURE 14. Characteristic silicoflagellate complex of the Neogene of northern Sakhalin (older complex): 1—3—Distephanus speculum var. cannopiloides (Pr.-Lavr.) Gleser; 4—6 — D. crux (Ehr.) Hack. var. crux; 7—Mesocena stellata Hack. This complex is comparable with the Middle Miocene silicoflagellate complex of the Calvert formation of the state of Maryland. Indeed, the proportion between D. crux (Ehr.) Hack. and D. speculum var. cannopiloides (Pr.-Lavr.) Gleser is almost the same in these com- plexes. Moreover, these elements of the Sakhalin and Maryland floras are morphologically identical. The abundance of D. crux (Ehr.) Hack. var. crux suggests a relation- ship between the above Sakhalin flora and the Late Miocene flora of the area of Hokuriku of Honshu Island (Japan), where D. crux (Ehr.) Hack. predominates (Ichikawa, 1956). However, the Sakhalin flora is more closely related to that of Maryland. 211 198 FIGURE 15. Silicoflagellate complex of the Neogene of northern Sakhalin (younger complex): 1—Dictyocha fibula Ehr. var. fibula f. fibula; D. f. var. pentagona Schulz; 3—Paradictyocha polyactis f. completa Freng.; 4—Distepha- nus speculum var. pentagonus Lemm.; 5—7—D. s. (Ehr.) Hack. var. specu- lum; 8—Paradictyocha polyactis f. mesocenoidea Freng.; 9— Distephanus speculum var. cannopiloides (Pr.-Lavr.) Gleser. The flora of the Hokuriku area of Japan (Tsukada horizon) resembles the complex of the Napana River, Kamchatka. D. crux (Ehr.) Hack. var. crux is the only abundant silicoflagellate in both localities; in addition to this form, the Napana flora consists of isolated specimens of D. speculum var. pentagonus Lemm. and var. cannopiloides (Pr.-Lavr.) Gleser. On the northern coast of the Shmidt peninsula (Machigar section), a different flora replaces the one outlined above. , This other, younger complex of Neogene silicoflagellates consists of varieties and forms of Dictyocha fibula Ehr., Distephanus speculum (Ehr.) Hack. and Paradictyocha polyactis (Ehr.) Freng. (Figure 15). Usually either Dictyocha fibula Ehr. var. fibula f. fibula or Distephanus speculum (Ehr.) Hack. var. speculum (sometimes var. pentagonus Lemm.) predominate in the flora. Sometimes these two species appear in equal amounts. Asa rule, the other forms are less abundant. The predominance of the warmwater Az species Dictyocha fibula Ehr. or the cold-water species Diste- phanus speculum (Ehr.) Hack. probably depends on the thermal regime of the basin. The flora described occurs on the northern, western and eastern coasts of the Shmidt peninsula, in the basins of the Kongi and Tumi rivers and of the Kongi River, as well as in Lake Machigar in northern Sakhalin, and in the Bryansk diatomite deposits in the southern part of the island and on the Kurile Islands. Distephanus speculum (Ehr.) Hack. var. speculum is by far the dominant form in the last two localities. According to Sheshukova-Poretskaya (1959), this silicoflagellate also predominates in the basins of the Nitui and Gurovka rivers in southern Sakhalin. In northern Sakhalin, D. speculum (Ehr.) Hack. var. speculum shares the dominant position with Dictyocha fibula Ehr. var. fibula f. fibula; these two forms sometimes are encountered in equal amounts. A Neogene flora analogous to that described is not known beyond the confines of the Soviet Far East, although some of its components are widespread in the Neogene of many areas. As in northern Sakhalin (the basins of the Troptun and Longi, and Kongi and Tumi), still another silicoflagellate complex has been found in southern Sakhalin (Pervomai area). This complex is dominated by Distephanus japonicus f. pseudofibula (Schulz) Gleser, which is very abundant in the Pervomai area and is somewhat less abundant inthe Shmidt peninsula. The remaining forms (Distephanus speculum (Ehr.) Hack. var. speculum, var. septenarius (Ehr.) Jorg. and var. cannopiloides (Pr.-Lavr.) Gleser, and Paradictyocha poly- actis f. mesocenoides Freng.) are represented by isolated or rare specimens and do not occur everywhere. The stratigraphic position of this complex is not quite clear. Its dominant form, Distephanus japonicus f. pseudofibula (Schulz) Gleser, is widespread in the Miocene. Analysis of publications and our own observations reveal the following characteristic of the silicoflagellate flora of the Neogene. In its generic composition, the Neogene flora resembles that of the Paleogene. Such genera as Dictyocha Ehr., Naviculopsis Freng., Distephanus Stohr, Cannopilus Hack. and Mesocena Ehr. persist during the Neogene together with two new monotypic genera, Paradictyocha Freng. and Notyocha Defl., and the genus Deflandryocha Jerk. On the other hand, the specific composition and, especially, the quantitative development of the Neogene silicoflagellate flora differ sharply from those of the Paleogene. The most widespread forms of the Paleogene are varieties of Dictyocha triacantha Ehr. and Naviculopsis bi- apiculata (Lemm.) Freng., whereas the genus Distephanus Stohr occurs in some localities only. During the Neogene a different picture prevails. Distephanus speculum (Ehr.) Hack. and D. crux (Ehr.) Hack., represented by several varieties and forms, are almost ubiquitous in the Neogene flora andoftenare dominant. The two new genera Paradictyo- cha Freng. and Notyocha Defl. as well as certain species (Diste - phanus japonicus (Defl.) Gleser, Dictyocha retrospina Defl., etc.), appearing in the Neogene are phylogenetically related to Diste- phanus speculum (Ehr.) Hack. Most of the species of Dictyocha 213 Ehr. known from the Paleogene (D. frenguellii Defl., D. transitoria Defl., D. rotundata Jousé, etc.) were not encountered in the Neogene. D. triacantha Ehr. is also widespread throughout the Paleogene but very rare in the Neogene, except in Japan where significant amounts occur (Ichikawa, 1956). Of the ancient species of Dictyocha Ehr., only D. fibula Ehr. persists in the Neogene. Two new species related to D. fibula Ehr. —D. mutabilis Defl. andD.ausonia Defl. — appear in the Neogene; the former is found in North America only, while the latter is known from Italy, California and Sakhalin. A variety of one of the most characteristic species of the Eocene flora (Naviculopsis biapiculata (Lemm.) Freng.) has been found in the Neogene only in North Africa (Oran) and southern Sakhalin. A peculiar form of this same species is encountered in southern Sakhalin (Sheshukova- Poretskaya, 1959). Moreover, N. iberica was described from the Neogene of Spain and N. rectangularis (Schulz) Freng. from the Miocene of Yugoslavia and Hungary. A few species of Mesocena Ehr. and Cannopilus Hack. are more widespread in the Neogene compared to the Paleogene. 199 Lower Quaternary silicoflagellates Quaternary silicoflagellates have not been studied specially, but numer- ous works dealing mainly with diatoms contain data on silicoflagellates of this period. Together with diatoms, the following silicoflagellates are regarded as indications of the marine interglacial deposits of the Gulf of Danzig (Schulz, 1928): Dictyocha Tibwul Ene var. TYbula t. “Mbures Distephanus speculum (Ehr.) Hack. var. speculum and var. septenarius (Ehr.) Jorg. Brander (1943) found skeletons of several silicoflagellate species in the interglacial deposits of the Karelian isthmus, in the area of Raukhiala village; most numerous are Distephanus speculum (Ehr.) Hack. var. speeurim and Dictyocha Tibula Ehr: var. frbula. “fibwPa, which he regards as characteristic of these deposits. Other varieties of Distephanus speculum (Ehr.) Hack. (var. pentagonus Lemm., var. septenarius (Ehr.) Jorg., var. cannopiloides (Pr.-Lavr.) Gleser) occur rarely. Of particular interest is the rare occurrence of specimens of Distephanus crux (Ehr.) Hack. in one of the samples. According to Brander, samples from deeper waters are richer in silicoflagellates, while there are few skeletons in deposits of the coastal zone. Isolated specimens of Distephanus speculum (Ehr.) var. spe- culum were found in the intermoraine deposits of the town of Povenets in the Karelian Autonomous SSR (Sheshukova-Poretskaya, 1955) and rare specimens were found by N. V. Anisimova (Sheshukova-Poretskaya, 1.c.) inthe intermoraine clays of the Mga River near Gora station in the Leningrad Region. Very rare amounts of Dictyocha fibula Ehr. var. fibula f. fibula and Distephanus speculum (Ehr.) Hack. occur in the intermoraine deposits of the watershed between the Tosno and Sablinka rivers in the Leningrad Region (Sheshukova-Poretskaya, l.c.). The same 214 200 species occur in marine intermoraine deposits of the Leningrad Region (collected by Stepanova and Chizhikova). According to Stepanova, both species are very abundant. Dictyocha fibula Ehr. var. fibula f. fibula is very abundant in the intermoraine stratum of the Lake Ladoga basin, Distephanus speculum (Ehr.) Hack. var. speculum is abundant and var. pentagonus Lemm. rare here (Cheremisinova, 1957). Very rare to rare skeletons of D. speculum (Ehr.) Hack. var. speculum occur in the interglacial deposits of the Dnieper-Valdai epoch of Karelia (Levina Gora and Vidlitsa) (Lak, 1959). Sheshukova-Poretskaya (1955) regards this species as part of the characteristic complex of micro- scopic algae associated with the marine intermoraine deposits of the European USSR. Kuptsova encountered isolated specimens of D. speculum (Ehr.) Hack. var. speculum inthe Folas transgression of the Kola peninsula. Zhuze (1959) reports one silicoflagellate species, Dictyocha (Dis- tephanus) octonaria Ehr. from horizon III of bottom deposits of the northwestern Pacific, as a component of the warmwater diatom complex of interglacial time. In a sample of interglacial Mga clays we found 2 silicoflagellate epecies — Dictyochsa. fibula Ebr var.itbulact. fibula and Distephanus speculum (Ehr.) Hack. var. speculum, both abundant. To sum up, the Quaternary silicoflagellate flora contains a modest number of species. The cold-water form Distephanus speculum. (Ehr.) Hack. var. speculum was the most abundant and widespread silicoflagellate during the Quaternary of northwestern Europe; in second place was the warmwater Dictyocha fibula Ehr. var. fibula f. fibula, although Distephanus speculum var. septenarius (Ehr.) Jorg. appears in considerable amounts in some localities. Dis - tephanus crux (Ehr.) Hack. var. crux and D. octonarius (Ehr.) Defl. can be characterized as very rare; the latter species is common to Quaternary marine deposits of the European USSR and the Pacific Ocean. All the silicoflagellate forms encountered in deposits of the Quaternary period are known from the Neogene. The Quaternary silicoflagellate flora is considerably impoverished in comparison with that of the Neogene. Not a single new form appeared during the Quaternary. Moreover, many species and genera which flourished in the Neogene apparently vanished during the Quaternary. Recent silicoflagellates The earliest descriptions of silicoflagellates of Recent seas appeared more than 100 years ago (Ehrenberg, 1841, 1844b). At present, most of the taxons established by Ehrenberg are only of historical interest. Descriptions, figures and data on the location of many Recent silico- flagellates can be found in the works of Schulz (1928) and Gemeinhardt (1930). Some publications dealing with the plankton of Recent seas contain descriptions and drawings of silicoflagellates (Hackel, 1887; Lemmer- mann, 1901b, 1903, 1908; Marshall, 1934; Gran et Braarud, 1935; 215 Gail, 1950; Gaarder, 1954; Frenguelli, 1960; Frenguelli and Orlando, 1958, etc.). Many studies of the plankton of the Recent seas include lists of silicoflagellates. Of particular value are publications containing exact information about temperature, salinity, depth and other environmental factors, as well as the amounts of silicoflagellates collected (Palibin, 1903 —1906; Linko, 1907, 1912; Gran, 1915; Kiselev, 1925, 1931, 1935a, 1939; Usachev, 1935; Braarud, 1945; Braarud, Gaarder and Gr¢gntved, 1953; Morozova-Vodyanitskaya, 1948, 1954; Gaarder, 1954; Kuz'mina, 1962b, etc.). Hovasse (1932, 1937) and Frenguelli (1935, 1938a, b) studied Recent silicoflagellates mainly in order to explain variations of their skeleton. Zhuze (1957, 1960, 1962) reports the presence of silicoflagellate skeletons in Recent deposits of Far Eastern seas. Of particular value is the article of Proshkina- Lavrenko (1959) on the silicoflagellates of the Black Sea. In addition to descriptions of the taxons, original drawings, indications on the occurrence and data on the ecology of the different forms, this article stresses the link between the Recent silicoflagellate flora and the ancient flora of the Black Sea basin. A list of silicoflagellates inhabiting Recent seas and oceans can be compiled from the pertinent literature. According to Deflandre (1950), only 3 species, each with varieties of its own, live in the plankton of Recent seas: Dictyocha fibula Ehr. typica (=var. fibula f. fibula),* f. aculeata Lemm. (= var. aculeata Lemm.), var. messanensis Lemm. (=var. messanensis (Hack.) Lemm.), var. stapedia Lemm. (= var. stapedia (Hack.) Lemm.), D. speculum Ehr. typica (= Distephanus speculum (Ehr.) Hack. var. speculum), var. regularis (=D. speculum var. regularis Lemm.), f. varians Gran et Braarud (= D. speculum f.. varians Gran et Braarud), and D. octonaria Ehr. typica (= D. octonarius (Ehr.) Defl. var. octonarius). This list, however, is not complete. Many authors (Hackel, 1887; Lemmermann, 1901b, 1903, 1908; Schulz, 1928; Gemeinhardt, 1930; Frenguelli, 1935; Gaarder, 1954; Proshkina-Lavrenko, 1959; Cassie, 1960) report the finding of Distephanus crux (Ehr.) Hack. var. crux. Schulz (1928) points out that this species is a common inhabitant of the plankton of the Adriatic Sea. Analysis of the preparation from Samarang (no. 3382 of the collection of H. Boecker) and examination of the drawings of D. crux (Ehr.) Hack. var. crux in the literature has convinced us that this silicoflagellate indeed lives in Recent seas. D. speculum var. pentagonus Lemm. occurs in the Atlantic and Antarctic oceans (Gemeinhardt, 1930, 1931a, 1934). Many investi- gators (Borgert, 1891; Jérgensen, 1899; Lemmermann, 1901b, 1908; Schiller, 1925; Gemeinhardt, 1930, 193la, 1934; Braarud, 1945; Gaarder, 1954; Kiselev, 1959b; Proshkina-Lavrenko, 1959; Paasche, 1960; Kuz'mina, 1962, and others) include D. speculum var. septenarius (Ehr.) Jorg. in their lists. Still another variety of D. speculum (Ehr.) Hack. — var. canno- piloides (Pr.-Lavr.) Gleser — occurs in plankton of Recent seas (Lemmermann, 1901b; Gemeinhardt, 1930, 1931a, 1934; Frenguelli and Orlando, 1958; Proshkina-Lavrenko, 1959, and others). 201 * The taxonomic terms accepted in the given work are noted in parentheses. 216 202 Distephanus octonarius var. polyactis (Jorg.) Gleser was found by several authors (Jorgensen, 1899; Lemmermann, 1903, 1908; Gemeinhardt, 1930, 193la, 1934; Proshkina-Lavrenko, 1959). D. octo- narius var. cyrtoides (Hack.) Gleser was found by Hackel (1887) in the central part of the Pacific Ocean and by us near the southern coast of Kamchatka. Several workers have found two forms of Dictyocha fibula var. messanensis —f. spinosa Lemm. (Lemmermann, 1901b; Gemein- hardt, 1930, 1934; Gaarder, 1954), andf. longispina Lemm. (Lemmermann, 1901b; Gaarder, 1954). Moreover, Gaarder (1954) encountered D. fibula var. pentagona Schulz, which had been regarded as extinct. The living specimen found by Gaarder differs from fossil skeletons in the presence of accessory spines (Gaarder, 1954, Figure 13). Mesocena stellata Hack. occurs in the central part of the Pacific Ocean (Hackel, 1887). Other species of Mesocena reported from Recent seas (Lemmer- mann, 1901b; Schulz, 1928; Gemeinhardt, 1930) require further study. The presence of Dictyocha navicula Ehr. and Cannopilus hemisphaericus (Ehr.) Hack. in Recent plankton may be doubtful, since skeletons of these silicoflagellates could have been washed out of ancient deposits. In his article Usachev (1947a) presents data on the total number of silicoflagellate species and their proportion in the algal plankton of northern, southern and Far Eastern seas. However, the figures in this work cannot be readily used since the author includes dinoflagellates among the silico- flagellates. At any rate, it is evident that the seas of the Soviet Union have a relatively poor silicoflagellate flora. Only one work (Proshkina-Lavrenko, 1959) deals in particular with the silicoflagellates of the seas of the USSR. Nevertheless, some idea of the species composition of the silicoflagellate flora can be obtained from a perusal of numerous publications. Nikolaev (1953) writes that in the open part of the Gulf of Riga, where salinity is 1.5% lower than in the open waters of the Baltic Sea, isolated specimens of Distephanus speculum (Ehr.) Hack. are encountered. However, this form appears in a depressed condition and does not repro- duce here. Several works contain lists of the silicoflagellates found in the northern seas of the USSR (Merezhkovskii, 1878; Reinhardt, 1882; Meunier, 1910; Palibina, 1903—1906; Linko, 1907, 1912; Kiselev, 1925, 1928, 1935a, 1939, 1957; Zabelina, 1930, 1946; Usachev, 1935, 1946, 1947b, 1949, 1961; Shirshov, 1937; Meier, 1938; Poretskii, 1939; Korotkevich, 1960). In the White Sea, in addition to D. speculum (Ehr.) Hack. var. speculum which is ubiquitous and sometimes appears in large amounts, sparse populations of D. speculum var. regularis Lemm. and Dictyocha fibula Ehr. var. fibula f. fibula are known. The plankton of the Barents Sea includes Distephanus speculum (Ehr.) Hack. var. speculum, var. regularis Lemm. and var. septenarius (Ehr.) Jorg. Moreover, D. speculum f. pseudo- fibula Schulz (= D. japonicus f. pseudofibula (Schulz) Gleser) was reported from these waters (Korotkevich, 1960). This form was hitherto regarded as extinct. The absence of a drawing makes a con- firmation of this diagnosis difficult. 217 203 D. speculum (Ehr.) Hack. var. speculum is the only form known from the Gulf of Pechora and Kara and East Siberian seas. D. speculum var. regularis Lemm. is the dominant silicoflagellate of Laptev and Chukchee seas, where it occurs together with very rare to rare specimens of D. speculum (Ehr.) Hack. var. speculum. D. speculum var. septenarius (Ehr.) Jorg. and var. octonarius (Ehr.) Jorg. (= D. octonarius (Ehr.) Defl. var. octonarius) were discovered in the plankton of the Arctic Ocean near the North Pole (Usachev, 1961). Isolated skeletons of these forms were also found ina sample of ice from the ''Papanin ice floe."' In addition to the review by Proshkina-Lavrenko (1959), information on the silicoflagellates of southern seas of the USSR can be found in a number of other works on the phytoplankton (Reingard, 1909; Usachev, 1927; Gemeinhardt, 1930; Mikhailovskaya, 1936; Stroikina, 1940; Morozova- Vodyanitskaya, 1940, 1948, 1954; Pitsyk, 1954). D. speculum (Ehr.) Hack. var. speculum andD. octonarius (Ehr.) Defl. var. octonarius were found in the Caspian Sea. The Black Sea has a more varied silicoflagellate flora: Dictyocha fibula! Ehr> van fibula’f. fibula, Distephanus le rx (Eee Hack. var. crux, D. speculum (Ehr.) Hack. var. speculum and var. septenarius (Ehr.) Jérg., D. octonarius (Ehr.) Defl. var. octo- narius andvar. polyactis (Jorg.) Gleser. Only isolated skeletons of D. speculum (Ehr.) Hack. var. speculum occur in the Sea of Azov. Information on the silicoflagellates of Far Eastern seas can be found in works dealing with the phytoplankton (Kiselev, 1931, 1935b, 1937, 1959a, b; Gail, 1950; Zabelina, 1953; Smirnova, 1956, 1959; Kuz'mina, 1959, 1962b; Semina, 1959, 1960) as well as in biological studies of Recent deposits of these seas (Zhuze, 1957, 1960, 1962). D. speculum var. regularis Lemm. and Dictyocha fibula Ehr. var. fibula f. fibula are known from the plankton of the Bering Sea. In surface sediments Distephanus crux var. stauracanthus (Ehr.) Lemm. (= D. stauracanthus (Ehr.) Hack.) and D. speculum var. octogena, D. speculum (Ehr.) Hack. var. speculum and Dictyocha fibula var. aculeata Lemm. were found. It is very probable that the first form does not occur in situ in these sediments, but was redeposited from more ancient deposits. From the plankton of the Sea of Okhotsk we know of Distephanus speculum (Ehr.) Hack. var. speculum and var. regularis Lemm., and D. octonarius (Ehr.) Defl. var. octonarius. Skeletons of Dictyocha fibula var. aculeata Lemm., Distephanus crux (Ehr.) Hack. var. crux, and D. speculum (Ehr.) Hack. var. speculum occur in the surface stratum of sediments. In the Sea of Japan occur Dictyocha fibula Ehr. var. fibula f. fibula, Distephanus speculum (Ehr.) Hack. var. speculum, var. cannopiloides (Pr.-Lavr.) Gleser and var. septenarius (Ehr.) Jorg., D. octonarius (Ehr.) Defl. var. octonarius, Canno- piloides hemisphaericus (Ehr.) Hack. and Mesocena circulus Ehr. The last two forms have probably reached the Sea of Japan waters from ancient sediments. From all these data, it appears that the most widespread species at present is Distephanus speculum (Ehr.) Hack., especially its type 218 204 variety. It is noteworthy that Dictyocha fibula var. aculeata Lemm., D. fibula var. messanensis (Hack.) Lemm. and its forms, as well as D. fibula var. stapedia (Hack.) Lemm. and Distephanus speculum f. varians Gran et Braarud are only known from Recent seas and do not occur in fossil state. 6. PHYLOGENY OF SILICOFLAGELLATES Schulz (1928) can be credited with the first attempt to trace the evolution of silicoflagellates. He has outlined, although very schematically, the main trend in the evolution of silicoflagellates from the simple triangular skeleton of the Paleogene representatives of Dictyocha Ehr. to forms with more complex skeletons (Distephanus Stohr and Cannopilus Hack.). Deflandre (1933a, 1936, 1940a, b, 1941, 1944, 1950, 1952a, b) devotes considerable attention to the evolution and phylogeny of silicoflagellates. According to Deflandre, the basic silicoflagellate type (the genera Corbisema Hannaor Dictyocha Ehr.) has persisted almost unchanged from the Cretaceous until the Recent epoch. All deviations from the original type proved less adaptable and vanished during evolution. Deflandre maintains that there are 3 trends in the evolution of the group. The first trend manifests itself in a reduction of basic parts of the skeleton, such as the basal ring or the apical apparatus. Thus, the loss of the basal ring in species of Corbisema Hanna during the Cretaceous created the regressive family Vallacertaceae Defl. According to Deflandre (1950, Figures 61—67) the skeleton of the genus Vallacerta Hanna is derived from that of Corbisema geometrica Hanna by a process of reduction to an apical plate and lateral rods. The genera Cornua Schulz and Lyramula Hanna are successive stages in the regression of a hypothetical species of Corbisema witha very high apical apparatus (Deflandre, 1950, Figures 69—79). Further, the loss of the apical apparatus in Tertiary silicoflagellates led to the formation of the genus Mesocena Ehr. emend. Defl. The second trend in the evolution of the group is related to changes in the form of the skeleton. Thus, the prototype of the genus Dictyocha Ehr. evolved into Naviculopsis Freng. with an elongated basal ring and into Cannopilus Hack. with a spherical skeleton. The third trend involves minor changes of the original skeleton. Examples are the loss of the tubular skeleton characteristic of the genus Phyllodictyocha Defl. and the formation of dentate ribs on the radial horns in the genus Nothyocha Defl. None of these trends have survived during the course of time, and genera which deviated from the highly successful prototype have become extinct. The only genus still alive today is Dictyocha Ehr.,* whose basic skeletal type has remained unchanged for more than 80,000,000 years (Deflandre, 1952b). A comparative study was made of silicoflagellate skeletons from Upper Cretaceous deposits of the eastern slope of the Urals, from Paleogene * Deflandre places all the species of Diste phanus Stdhr in the genus Dictyocha Ehr. 219 (205) rajdwis vjnwoshT pynoinf vpnuoshT | | | piaflajnap vnUusLOD pyDIANf14y VNULOD 21U07L0Y D}4900]10 4 aplvyzjaiod vnusog pyjuvoni} vYyI0h}I1Gq 1DUUDY DI19ID]]D 4 xrajdwis 0}4090]]0 A DINP1IUWN} Vj19ID]]0 A bar | | | SS eee et ee, 1, pupiysjasuvyoiv vyv0hj01q aan : | | | | ppnajavu vysoh121¢q D]D)}a i eee pid{i]]awuD] eel pyv0hj01po)] hyd pyvoin{ vysohyorg vsouids vy20hj01q A | Plt ER l “N pingif vyo0hqo1q pyjuvovxay vyv0h}01q pyvsuoja vy20h}01Gq | raipuvjf{ap vyvohja1q.- dpjansuasf vyv0hj21Gq pisngot sisdoj]no1avy | Oe | rnaa snuvydajsig pyppunjo4 vyvohj21q pyppnaidvig sisdoj]no1av \] wnjnoads snuvydajsiq py1ojysunsy DYyI0NIOIG | Ae ike et es eae a eer snoiuodv{ snuvydajsiq snnbiqupv snuvydajsiq paan1jof sisdojno1anAy sniipuojv0 snuvydajsiq vzijosur vyoohyioN sijovhjod vys20hj01pvsvg SALVTISDVISODITIS JO VUINIO GNV SAIOIdS ANOS JO ANAOOTAHd IHL JO AWAHOS 2 w 206 sediments of the Ukraine, the Volga area, the eastern slope of the Urals and the West Siberian plain, from Neogene rocks of the Northern Caucasus, Kamchatka, the Kurile Islands, Sakhalin, and from Quaternary deposits of the Leningrad Region. This research, together with a review of publications, revealed the phylogenetic links between certain genera and species (see scheme) and showed the successive stages in the evolution of the group. In a number of points, our results diverge from the views of Deflandre. Paleontological evidence does not conclusively indicate that Dictyocha Ehr. (or Corbisema Hanna, according to Deflandre) is the earliest silicoflagellate genus. No thorough study has yet been made of Lower Cretaceous silicoflagellates. The accidental findings of skeletons of Dictyocha triacantha Ehr. in the Lower Cretaceous of Germany indicate merely that this is an ancient species. The abundance of Corbisema geometrica Hanna in the Maestrich- tian of California (Deflandre, 1950; Mandra, 1960) also is not proof of its greater antiquity than the families Cornuaceae Gem. or Vallacertaceae Hanna. Indeed, Vallacerta Hanna and Lyramula Hanna are abundant in the Maestrichtian of California, while the dominant complex of the Santonian-Campanian of the eastern slope of the Urals consists entirely of members of the families Vallacertaceae Defl. and Cornuaceae Gem.; species of Dictyochaceae Lemm. occur in this complex much less fre- quently and in negligible amounts. The abundance and wide distribution of Lyramula Hanna and Cornua Schulz in Upper Cretaceous deposits, as well as the primitive structure of their skeletons, indicate that the original family is Cornuaceae Gem., and not Dictyochaceae Lemm. as Deflandre (1950) believes. My own views (Glezer, 1959) on this topic agree with those of Proshkina-Lavrenko (1959). In the course of evolution, the divisions of the class Silicoflagellato- phyceae do not occupy equivalent positions. Thus, the monotypic family Vallacertaceae Defl. stands far apart from the rest of the class. In con- trast to the remaining silicoflagellates, the skeleton of species of Valla - certa Hanna consists of a continuous, undifferentiated polygonal plate from whose corners usually arise hollow outgrowths resembling radial horns. Because of the external similarity of the skeleton of this genus and the apical apparatus of Corbisema geometrica Hanna, Deflandre (1950) regards the polygonal plate of Vallacerta as an apical plate. Since no direct relationships have been established between the genus Vallacerta Hanna and the other silicoflagellate genera, there is no justification for interpreting the skeleton of this genus as homologous to skeletal formations of other silicoflagellates. No trace of a silicoflagellate related to the genus Vallacerta Hanna has been found in much later sediments. This genus probably represents a blind alley of development. The evolution of the 4 known species of Vallacerta is essentially confined to the Upper Cretaceous. Morpho- logically, these species are now close to one another, which undoubtedly reflects an intimate phylogenetic link. The wide range and abundant occurrence of V. hortonii Hanna suggests that this species may be more ancient than the rest. It is possible that it gave rise to V. tumidula Gleser by minor changes in the structure of the plate and to V. simplex Jousé by a reduction of the radial horns. The latter two species have a relatively small range — the eastern slope of the Urals — and are abundant 221 207 208 in some localities only. These features suggest a greater specialization and probably a younger age than V. hortonii Hanna. The same con- siderations apply to the Californian species V. hannai Defl. Almost all the remaining silicoflagellate genera have a skeleton consisting of hollow siliceous rods. All these genera have a common origin. The Cretaceous genus Lyramula Hanna of the family Cornuaceae Gem. has a skeleton of the simplest type consisting of U- or Y-shaped rods. From the Upper Cretaceous deposits of California, Deflandre (1950, Figures 167, 173) described skeletons of Lyramula sp. with 3 rods forming a dome characteristic of silicoflagellates; we have observed such skeletons in samples from the eastern slope of the Urals (Figure 16, 3). These findings indicate that the Lyramula skeleton is homologous to the apical apparatus of other, more advanced silicoflagellates. Such skeletons with 3 rods provide a phylogenetic link between Lyramula Hanna and another genus of the same family — Cornua Schulz (Figure 16, 1—5). Species of Lyramula, suchas L. furcula Hanna and L. simplex Hanna, are characterized by a wide geographical range and a comparatively brief period of existence. Abundant and widespread fossils of these forms occur only in the Upper Cretaceous of California and the eastern slope of the Urals; both species disappear at the beginning of the Tertiary. Unlike Vallacerta Hanna, the genus Lyramula Hanna represents a progressive stage in the evolution of silicoflagellates. Further modifica- tion of the Lyramula skeleton during the Cretaceous leads to differentia- tion of the genus Cornua Schulz. In this genus, the apical rods already form the true dome typical of silicoflagellates on the whole (Figure 16, 4, 5) and there are well developed supporting spines and rudiments of a basal ring. There are only 3 known species: C. aculeifera Defl. described from the Upper Cretaceous of California and very rarely encountered in Upper Cretaceous deposits of the eastern slope of the Urals; C. trifurcata Schulz known from the Senonian of the Gulf of Danzig and the eastern slope of the Urals; and the rare species C. poretskajae Gleser encountered in only 2 localities of Sverdlovsk Region. The first two species are rather specialized morpho- logically, while C. poretskajae Gleser represents a more progressive stage in the evolution of silicoflagellates. Indeed, a form of the type of C. poretzkajae Gleser could readily be a transition to Dictyocha triacantha var. inermis Lemm. f. inermis through coalescence of the basal rods into the basal ring characteristic of the family Dictyo - chaceae Lemm. (Figure 16,6). This hypothesis is supported by the finding of skeletons of Cornua poretzkajae Gleser together with skeletons of Dictyocha triacantha var. inermis Lemm. f. inermis and by the roughly equal size of these structures. Moreover, the corners of the basal ring of some ancient D. triacantha skeletons bear a thin band, probably a trace of the fusion of the basal rods. Thus, the Mesozoic witnesses the appearance of Dictyocha Ehr., one of the most species-rich genera of the family Dictyochaceae Lemm., especially during the Paleogene. Zon (207) ‘ ls 7 a 5 Shs FIGURE 16. Phylogenetic links between the families Cornuaceae Gem. and Dictyochaceae Lemm.: 1—Lyramula simplex Hanna; 2—L. furcula Hanna; 3—Lyra- mula sp.; 4,5—-Cornua poretzkajae Gleser; 6—Dictyocha triacantha var, inermis Lemm. f. inermis. Dictyocha Ehr. occurs very rarely (isolated specimens) in the Santonian-Campanian of the eastern slope of the Urals. It is represented there mainly by different forms of a single species — Dictyocha tria- Cantha Ehr. > ihe simplest of itse is Do triacauntna var. inernis Lemm. f. inermis. Close relations of this form, D. triacantha War. apteulard Lewmm. 1. adhbiculatia angi. late-radiata, are already equipped with radial horns, though very short ones; D. tria- cantha var. apiculata f. late-radiata Schulz has features in common with Corbisema geometrica Hanna, which is not known in the Santonian-Campanian of the eastern slope of the Urals but occurs in large amounts in the Maestrichtian of California. A variety of silico- flagellates of the family Dictyochaceae have been described from the Upper Cretaceous deposits of the Gulf of Danzig. However, the lack of quantitative data makes it difficult to use these materials for an analysis of the development of the silicoflagellate flora. 223 209 FIGURE 17. Phylogenetic relationships of some species of the genus Dictyocha Ehr.; 1—Dictyocha triacantha var. inermis Lemm. f. inermis; 2, 3— D. navicula Ehr. (2 —after Deflandre, 1950); 4—D. archangelskiana (Schulz) Gleser; 5—D. furcata Jousé. The domination of the family Dictyochaceae Lemm. begins in the Tertiary. Dictyocha triacantha Ehr., represented by several varieties, is by far the dominant silicoflagellate in the Early Paleocene of the eastern slope of the Urals and the Volga area. Although this species was already present throughout the Tertiary, its morphogenetic and quantitative proliferation are associated with the Paleocene. D. tria- cantha Ehr. is the ancestor of many other species of the genus. Rich material from the Early Oligocene indicates that D. triacantha var. inermis Lemm. f. inermis gave rise to D. archangelskiana (Schulz) Gleser by a gradual change in the contour of the basal ring (Figure 17, 4). A succession of transitional forms connect the latter species with D. triacantha var. inermis Lemm. f. inermis during the Early Paleocene; only the extreme forms differ sharply from one another. 224 210 D. archangelskiana (Schulz) Gleser already appears as an inde- pendent species in the Late Eocene — Ear.y Oligocene of Oamaru (New Zealand). Materials from the Paleocene of the eastern slope of the Urals prove the phylogenetic relationship between D. archangelskiana (Schulz) Gleser and D. furcata Jousé (Figure 17, 5). The latter species is confined in time to the Upper Cretaceous — Early Paleocene and in space to the eastern slope of the Urals. During the Early Eocene, the varieties of D. lamellifera Gleser replace those of D. triacantha Ehr. as dominant elements of the silico- flagellate complex. Both species are tripartite in structure, which reflects their mutual relationship (Figure 18, 1—3). However, D. lamellifera Gleser differs from D. triacantha Ehr. in the presence of flattened areas on the basal rods, and a reduction of the supporting spines in some specimens. Close to D. lamellifera Gleser is another Early Eocene species, D. elongata Gleser, which occurs as a frequent form on the eastern slope of the Urals and as a rare form in the Volga area. Along with a total lack of the supporting spines, a gradual reduction of 2 of the 3 lateral rods and of 1 radial horn, and a modification of the basal ring from a triangle to a boat shape are observed in this species (Figure 18, 4—8). Dictyocha elongata Gleser provides a direct phylogenetic link between the genera Dictyocha Ehr. and Naviculopsis Freng. Another regressive form of the genus Dictyocha Ehr. is D. navi- cula Ehr. The bilaterally symmetrical cell of this species is derived from that of D. triacantha var. inermis Lemm. f. inermis bya partial reduction of the skeleton (Figure 17, 1—3). Deflandre (1946, 1950) demonstrated a direct connection between these two forms. During the Early Eocene, D. navicula Ehr. occurs in moderate quantities over a considerable range which includes Denmark, the Volga area, the eastern slope of the Urals and the Trans-Urals. Skeletons of this species are known from the Miocene of Zante Island (Greece), but differ morpho- logically from those found in the Paleogene. A form with a quadrangular basal ring which evolved from D. tria - cantha Ehr. (Figure 19, 1) during the Early Eocene is D. fibula var. fibula f. eocaenica Krotov (Figure 19, 2). There can be no doubt as to the phylogenetic relationship between these two silicoflagellates. Indeed, D. fibula var. fibula f. eocaenica Krotov so closely resembles D. triacantha Ehr. in the nature and arrangement of the supporting spines that Frenguelli (1940) regarded it as a dictyochalike form of Corbisema (=Dictyocha)triacantha. (Ehr.)\Freng..and C. apiculata (Lemm:) Frengs(= D. triacantti@ Bhr-): D. fibula var. fibula f. eocaenica Krotov occurs in the Early Eocene of Denmark and the eastern slope of the Urals. This form is frequently dominant in many parts of the Sverdlovsk Region, but quantitative data on its development in Denmark have not been published. D. fibula var. fibula f. eocaenica Krotov may possibly be the ancestor of D. fibula Ehr., whose other varieties are widespread in our day. D.triacantha Ehr. (Figure 19, 1) produced yet another species during the Eocene — D. elata Gleser (Figure 19, 4—6), whose original variety (D. elata Gleser var. elata) closely resembles D. triacantha Khe war. triacantha f. triacantha,: but differs from it in the structure of the lateral rods. In relation to this, the appearance of a new 225 skeletal feature during the Eocene must be noted, namely, the nearly perpendicular position of the lateralrods with respect to the plane of the basal ring. FIGURE 18. Phylogenetic relationships between the genera Dictyocha Ehr. and Navi- culopsis Freng.; 1—Dictyocha triacantha Ehr. var. triacantha f. triacantha; 2—D. lamel- lifera Gleservar.lamellifera; 3—D. l. var. constricta Gleser; 4—8 —D. elongata Gleser; 9—Naviculopsis robusta Defl.; 10—N. biapiculata (Lemm.) Freng. var. biapiculata; 11—N. b. var. minor (Schulz) Gleser; 12—N. foliacea Defl. 226 211 FIGURE 19. Phylogenetic relationships among some species of the genus Dic - tyocha Ehr.; 1—Dictyocha triacantha Ehr. var. triacantha f, triacantha; 2— D. fibula var. fibula f. eocaenica Krotov; 3—D. f. Ehr. var. fibula f. fibula; 4—D. elata Gleser var. elata; 5—D. e. var. media Gleser f. media; 6—D. e. var. media f. reducta Gleser; 7—D. spinosa (Defl.) Gleser; 8—D. hexacantha Schulz. D. elata Gleser var. elata is especially abundant in the Middle (?) Eocene deposits of the eastern slope of the Urals and the West Siberian plain. It occurs very rarely in the Upper Eocene and Upper Eocene — Lower Oligocene (?). This variety is also known in the Early Eocene of Denmark. Its quantitative occurrence is unknown. In the Early Oligocene (?) of the West Siberian plain this species produced two regressive forms — var. media Gleser f. media and var. media f. reducta Gleser, which occur very abundantly (Figure 19, a, a). 227 During the Early Oligocene (?) of the northern part of the West Siberian plain, D. elata var. media Gleser f. media produced a new species, D. spinosa (Defl.) Gleser (Figure 19, 7). A series of transitions relate the new species with the ancestral form here; only in the Paleogene of other regions (Kharkov suite, Oskol River in the Ukrainian SSR, the upper part of the Tas- Aran suite of the Uzen -Kairakty River, a right tributary 21 of the Irgiz River) and in the Late Eocene — Early Oligocene of Barbados Island (Lesser Antilles) can D. spinosa (Defl.) Gleser be regarded as an independent form. FIGURE 20, Phylogenetic relationships of some species of the genus Dictyocha Ehr.; 1—Dictyocha elata Gleser var, elata; 2—D. deflandrei var. completa Gleser f. completa; 3—D. d. var, completa f. producta Gleser; 4—D. d. var, bicornuta Gleser; 5—D. obliqua Gleser; 6—D. frenguellii var. car- entis Gleser f. carentis; 7—D. f. var. carentis f. incerta Gleser; 8—D. rotundata Jousé var. rotundata; 9—11—D. r. var. secta Gleser; 12, 13— transitional forms from D. fren guellii Defl. toD. transitoria Defl.; 14—D. transitoria Defl. This evolutional series ends in D. hexacantha Schulz (Figure 19, 8). The evolution from D. spinosa (Defl.) Gleser to D. hexacantha Schulz apparently involves a partial reduction of the lateral rods and 228 213 afusionofthe accessory spines with the basal ring. Skeletons of both species occur together in Paleogene deposits (Kharkov suite of the Dnieper- Donets depression; Uzen'-Kairakty River, the northwestern part of the Turgai Gates), which suggests that D. hexacantha Schulz appeared in the Paleogene. The finding of this species in the Upper Eocene or Lower Oligocene of Oamaru (New Zealand) indicates its extensive distribution in the Paleogene. D. hexacantha Schulz existed until the Late Paleogene — Early Neogene (the Late Eocene — Early Miocene of Barbados Island in the Lesser Antilles). Another line of evolution arises from D. elata Gleser during the Eocene. The new species D. frenguellii Defl. appeared at the beginning of the Eocene, apparently arising from D. elata var. elata Gleser through a sudden increase in the number of the skeletal elements. D.fren- guellii Defl. occurs in the Eocene of the Volga area and Western Siberia (Figure 20, 6, 7). We do not possess any quantitative data con- cerning the Volga area. In Western Siberia, one variety (var. frenguel - lii) of this species appears in large amounts in Late Eocene deposits only in a few areas of the eastern slope of the Urals and the West Siberian plain; another variety (var. carentis Gleser) is abundant almost every- where from the Middle (?) Eocene to the end of the Late Eocene — Early Oligocene (?). A tendency toward a reduction of the radial horns and a more rounded skeletal form is evident even within this species. Large amounts of skeletons of D. frenguellii var. carentis f. incerta with almost reduced radial horns occur in the Late Eocene and the Late Eocene — Early Oligocene (?) almost throughout the surveyed parts of the West Siberian plain and the eastern slope of the Urals. The above form phylogenetically links D. frenguellii Defl. with D. rotundata Jousé (Figure 20, 8—11). The oldest form of D. rotundata Jousé — var. rotundata Gleser — is closely similar morphologically to DO Trengvwell ti-war. careéntis. foiinc erranieser, Dr rotundata Jousé var. rotundata dominates in the Late Eocene— Early Oligocene (?) of Western Siberia, but declines in the Early Oligocene (?). Another form, Dictyocha rotundata var. secta Gleser, de- veloped from the type form by a division of the lateral rods (Figure 20, 9—11), reaches a quantitative peak in the Late Eocene — Early Oligocene (?) and the Early Oligocene (?) of the same areas. D. transitoria Defl. also evolved from D. frenguellii Defl., but in a different direction. This species actually developed from D. fren- guelliivar. carentisGleser f. carentis by a lengthening of the basal ring and a reduction of two lateral radial horns (Figure 20, 6, 12— 14); it occurred on the eastern slope of the Urals and on the West Siberian plain from the Early Eocene to the Early Oligocene (?), reaching a peak in the Late Eocene and the Late Eocene — Early Oligocene (?). D. tran- sitoria Defl. is also known from the Eocene of the city of Kuznetsk in the Volga area. D. deflandrei Freng. with its several varieties is widespread in the Eocene. Morphologically, this species closely resembles D. frenguellii Defl. Transitional forms between D. frenguellii var. carentis Gleserf. carentis and D.deflandrei var. completa Gleser f. 229 completa occurred frequently in the Late Eocene and Late Eocene — Early Oligocene (?) of Western Siberia. Like D. frenguellii Defl., D. deflandrei Freng. shows a tendency toward lengthening of the skeleton and reduction of two lateral radial horns (D. deflandrei var. completa f. producta Gleser and D. deflandrei var. bicornuta Gleser) (Figure 20, 3— 4). The existence of transitional forms between D. deflandrei var. completa Gleserf. completa and D. fibula Ehr. var. fibula makes it difficult to solve the problem of the origin of D. deflandrei Freng. D. obliqua Gleser from the Late Eocene — Early Oligocene (?) of Western Siberia is a short-lived relation of D. deflandrei Freng. (Figure 20, 5). Several trends of evolution arise from the genus Dictyocha Ehr. One of these leads to the Early Eocene genus Naviculopsis Freng. As already mentioned, the gradual accumulation of regressive signs began already within the genus Dictyocha Ehr., which set the course for the evolutionary series D.triacantha Ehr. —D.lamellifera Gleser — D. elongata Gleser. The latter species is directly connected to Naviculopsis robusta Defl. (Figure 18, 9), also known from the Early Eocene of the eastern slope of the Urals, the Trans-Urals and the Volga area. The tubular nature of the skeleton of N. robusta Defl. is more pro- nounced than in any other species of Naviculopsis, and only small areas of the basal rods are flattened init. Further reduction of the inner canal and flattening of skeletal elements are observed in the varieties of N. biapiculata (Lemm.) Freng. (Figure 18, 10,11). Thus, only some parts of the basal rods are flattened in the skeleton of N. biapiculata (Lemm.) Freng. var. biapiculata, while invar. minor (Schulz) the inner canal is reduced even in the apical rod. These two varieties occur together and in small amounts in the Early Eocene of the eastern slope of the Urals, but are often dominant in the Middle (?) and\Late Eocene of the eastern slope of the Urals and the West Siberian plain. N. biapi- culata (Lemm.) Freng. also predominate in the Late Eocene silico- flagellate complex of California (Mandra, 1960). Further flattening of the skeletal elements during the Late Eocene — Early Miocene leads to N. foliacea Defl., known from Barbados Island in the Lesser Antilles (Figure 18, 12). The presence of skeletons with a very wide apical rod in N. biapiculata var. minor (Schulz) Gleser confirms the phylogenetic link between it and N. foliacea Defl. (Figure 18, 11). The origin of N. trispinosa (Schuiz) Gleser is obscure; this species may be a side branch in the evolution of N. bi- apiculata (Lemm.) Freng. Still another genus, Phyllodictyocha Defl., can be traced back to Dictyocha Ehr. Here the evolutional changes affect only the structure of the skeleton, which in Phyllodictyocha Defl. consists of flat, solid rods without an inner canal. As far as the form of the skeleton is concerned, both species of this genus — Ph. recta (Schulz) Defl. and Ph. schulzii Defi. from the Late Eocene — Early Miocene of Barbados — closely re- semble D. triacantha Ehr. Further evolution of silicoflagellates led toward modification of the apical apparatus. Already in the Eocene, genera suchas Distephanus Stohr and Cannopilus Hack. are known, in which the BPIee, apparatus is far more complex than in Dictyocha Ehr. 214 230 15 The close relationship between the genera Dictyocha Ehr. and Distephanus Stohr. was stressed by Lemmermann (1901b) and Gemeinhardt (1930); Frenguellii (1940) and Deflandre (1950) even deny the generic rank of Distephanus Stohr and place its species in the genus Dictyocha Ehr. Gemeinhardt (1930, p. 24, Figure 8a, b) explains the formation of the genus Distephanus Stohr from Dictyocha Ehr. thus: an opening could readily appear in the widened apical plate of D. fibula var. fibula f. rhombica Schulz, creating the species Distephanus crux (Ehr.) Hack. Another essential condition for such development is the formation of an inner canal in the remaining part of the apical plate, since the apical ring of all species of Distephanus Stohr is invariably tubular. On the other hand, D. crux (Ehr.) Hack. could also have evolved from Dictyocha deflandrei Freng., which has a very wide apical plate. D. speculum (Ehr.) Hack. probably developed from D. crux (Ehr.) Hack. by an increase in the number of skeletal elements. The phylogenetic relationships of D. antiquus Gleser are not quite clear. The skeleton of this species has essentially the same pattern as D. speculum (Ehr.) Hack., although some of its features are reminiscent of Dictyocha rotundata Jousé. Skeletons of Distephanus anti- quus Gleser occur in the Early Oligocene (?) deposits of the northern part of the West Siberian plain and in the Late Eocene deposits of the Aral area. D. crux (Ehr.) Hack. is extremely rare in the Early Oligocene (?) deposits of the West Siberian plain. Numerous skeletons of this species occur in the Paleogene of the Uzen'-Kairakty River (a tributary of the Irgiz River), in the Neogene of the Caucasus (Maikop series), the Sar- matian stage of the Dnepropetrovsk Region, the Neogene of Sakhalin (lower part of the Diatom suite), and in the Miocene of North America. In the two latter localities, D. crux (Ehr.) Hack. is not only dominant, but shows marked morphological diversity. Only isolated specimens of this species are known from the Lower Quaternary and from Recent seas. Another species of Distephanus Stohr, — D. speculum (Ehr.) Hack. represented by several forms, appeared during the Late Eocene. For the Late Eocene of Western Siberia only isolated occurrences of D. speculum (Ehr.) Hack. var. speculum are known. D. speculum var. pentagonus Lemm. also appears very rarely in the Late Eocene and Early Oligocene (?) of Western Siberia; small amounts of this variety occur in the Paleogene of the Uzen'-Kairakty River, together with isolated specimens of D. speculum var. cannopiloides (Pr.-Lavr.) Gleser. All these forms of D. speculum (Ehr.) Hack. are known from the Late Eocene or Early Oligocene of California (Krayenhagen formation). D. speculum (Ehr.) Hack. becomes especially diverse and abundant in the Neogene. Thus, D. speculum (Ehr.) Hack. var. speculum often predominates in the Neogene of Sakhalin, Kamchatka and the Kurile Islands. D. speculum var. cannopiloides (Pr.-Lavr.) Gleser, a silicoflagellate of considerable morphological diversity, is widespread in the Neogene of various parts of Europe, Sakhalin and America. Only one variety — D. speculum (Ehr.) Hack. var. speculum — can be characterized as widespread and abundant in the Lower Quaternary, at least in some areas. The skeleton of this variety is distinguished by its morphological stability. 231 Two lines of evolution arise from D. speculum (Ehr.) Hack. in the Neogene. Reduction of the apical ring of D. speculum (Ehr.) Hack. var. speculum (Figure 21, 1) leads to the regressive species D. japonicus (Defl.) Gleser with 2 forms (Figure 21,5—9), one of which, D. japonicus f. japonicus, appears to be confined to the Pacific zone (Sakhalin, Japan), and occurs very rarely on Sakhalin. The second form, f. pseudo- fibula (Schulz) Gleser, has a wider range which includes the Neogene of Europe. (216) FIGURE 21. Phylogenetic relationships between the genera Distephanus Stohr and Paradictyocha Freng. 1—Distephanus speculum (Ehr.) Hack. var. speculum; 2—D.s. var. septenarius (Ehr.) Jorg; 3—D. octonarius var. polyactis (Jorg.) Gleser; 4—Paradictyocha polyactis f. completa Freng.; 5-7 — Distephanus japonicus f. pseudofibula (Schulz) Gleser; 8, 9—D. j. (Defl.) f. japonicus. In the other line of evolution, D. octonarius (Ehr.) Defl. evolved from D. speculum (Ehr.) Hack. by an increase in the number of skeletal elements (Figure 21, 1—3). This species is rather rare both in the Neogene and in Recent seas. D. octonarius var. polyactis (Jérg.) Gleser provides a phylo- genetic link between Distephanus Stohr and the closely related mono- typic genus Paradictyocha Freng. (Figure 21, 4). Both forms of P. polyactis (Ehr.) Freng. are widespread in the Neogene, although they occur rather rarely in the Neogene of Sakhalin. 232 216 217 Distephanus Stohr gave rise during the Neogene to another monotypic genus, Nothyocha Defl. Its species, N. insolita Defl., is known from the Miocene of Italy; morphologically, it closely resembles Distephanus speculum (Ehr.) Hack. var. speculum. The genus Cannopilus Hack. has an even more complex apical apparatus than Distephanus Stohr. Several authors who have worked with Neogene materials (Schulz, 1928; Gemeinhardt, 1930) maintain that these two genera are closely related. A species of this genus, Cannopilus hemisphaericus (Enhr.) Hack., proved to be a more ancient species than hitherto believed. It occurs, though rather rarely, in the Late Eocene of the West Siberian plain. However, no transitional forms were found there between this species and species of other genera. Another species, C. sphaericus Gem. with a more complex skeleton, is known only from the Miocene of Hungary and the Neogene (?) of California. The origin of this species remains obscure. The species, C. ernestinae Bachmann, C. picassoi Stradner, C. schulzii, etc., are known only from the Neogene of various countries. With respect to the genus Mesocena Ehr. emend. Defl., the published data are too contradictory and our own experience too limited to attempt to trace its phylogenetic links. This genus may indeed be a collective one, comprising species of polyphyletic origin. To sum up, the families Vallacertaceae Defl. and Cornuaceae Gem. predominates during the Upper Cretaceous. The genus Cornua Schulz provided a phylogenetic link between the latter family and Dictyochaceae Lemm., which flourished during the Tertiary. Most species of Dictyocha Ehr., the oldest genus of the family, appeared during the Paleogene. During the Paleogene, Dictyocha Ehr. gave riseto the genera Diste- phanus Stohr and Naviculopsis Freng.; the latter is typical of the Paleogene. Species of Distephanus Stohr and Cannopilus Hack. flourished during the Neogene. During the same period, Distephanus Stohr produced the new genera Nothyocha Defl. and Paradictyocha Freng. Only a few species of two genera, Dictyocha Ehr. and Distephanus Stohr, persisted in the Lower Quaternary. These same members of the family Dictyochaceae populate Recent seas and oceans. 5698. 216—7.151. JH 6.70 233 218 tr) «~SYSTEMATIC PART Phylum CHRYSOPHYTA Class SILICOFLAGELLATOPHYCEAE BORGERT Silicoflagellatae Borgert (1891), Z.wiss. Zool., Bd. 51, p. 663. Microscopic, unicellular, autotrophic, uniflagellate marine planktonic algae with an internal, usually hollow, siliceous skeleton of more or less regular geometric form. Key to the Orders I... Skeleton consists of a flat, undifferentiated plate: =. w6).e./asi@obet rote Moe tae Fier aathel ot aeowlod Atk Vallacertales (p. 234), II. Skeleton composed of tubular rods ..... Siphonotestales (p. 236), Order VALLACERTALES Gleser Skeleton consists of an undifferentiated polygonal plate. Family VALLACERTACEAE Defl. emend. Gleser Vallacertidae Deflandre (1950), Microscopie, 2, p. 48. Skeleton represents a polygonal plate. Genus 1. Vallacerta Hanna *Hanna (1928), J. Paleontol. 1, 4, p. 262; Deflandre (1950), Microscopie, 2, p. 57; Glezer (1959), Inform. sb. VSEGEL, 10; jp. *10e: * (Description citations are as given in the original Russian text. The reader should note that the term "Table" can also refer to plates or pictures. ] 234 Skeleton consists of a polygonal, convex apical plate with narrow hyaline margin and with radial horns arising from the corners of the plate. The plate surface bears a conspicuous fine reticulate pattern of ribs and nodules. Type: Vallacerta hortonii Hanna. Extinct marine genus. Key to the Species of the Genus Vallacerta I. Plate uniformly slightly convex ie. vee ors Ones <7 2,55 elgee ax pk ee fa sks Vi. horton... Owe adie] shorns Fug Ment Bey, pres me! ee mrest oldie . V. simplex 2. i. Plate; center with,voundedsGonvexraTean mane, site smver ayn V. tumidula 3. 1. Vallacerta hortonii Hanna (Plate I, 1; Plate XXXI, 1). Hanna (1928), J. Paleontol. 1, 4, p. 262, Table 41, Figure 7, 11; Deflandre (1936), Actual. scient. ind. 335, p. 32, Figure 43; Deflandre (1940), C. r. Hebd. Seance Acad. Sci. 211, 19, p. 446, Figures 1,5; p. 598, Figure 1; Deflandre (1950), Microscopie, 2, p. 57, Figures 144— 149; Zhuze (1949), Bot. mater. Otd. spor. rast. BIN AN SSSR, 6, 1—6, Table 2, Figure 6; Glezer (1959), Inform. sb. VSEGEI, 10, p. 106, Figure 2; Krotov and Shibkova (1961), Mater. po geol. i polezn. iskop. Urala, 9, Figure 2, 19. — Dictyocha siderea Schulz (1928), Bot. Arch. 21, 2, p. 284, Figure 81; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 56, Figure 47. — D. siderea var. quadrata Schulz (1928), Bot. Arch. 21, 2, p. 284, Figure 82; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 57, Figure 48. Skeleton consists of a pentagonal, occasionally quadrangular or hexagonal, convex apical plate with bluntly rounded, sometimes produced corners and almost straight or concave sides, 15—25 yu long, with a narrow hyaline margin. Radial horns are hollow, 3—25y long, often unequal in length and frequently one is almost twice as long as the rest. Sculpture consists either of nodules and ribs arranged in a network or of fused, unevenless distri- buted dots. Distributioninthe USSR: Santonian-Campanian. Western Siberia: eastern slope of the Urals and the Trans-Urals, Slavgorod suite, very rare to abundant (Nes'-Yugan River, left tributary of the Synya River; basin of the Severnaya Sosva, Ust'-Man'ya village; Leplya and Nyais rivers; basin of Loz'va River, Pristan' village; Pelym River; Ivdel', Serov and Verkho- tur'e areas; Bol'shoi and Poludennyi Aktai rivers; Tynya River, Berezovo area); Kazakhstan: Kustanai Region, Kushmurun area, rare. Early Paleocene. Western Siberia: eastern slope ofthe Urals, Makhnevo and Ivdel' areas, lower part of Talitsa suite, very rare. General distribution: Senonian. Central Europe (Poland, Gulf of Danzig). Maestrichtian. North America (California, Moreno shales). Note: The report concerning the presence of this species in the Miocene of Nankoori, India (Desikachary and Maheshwari, 1956, p. 260, text-figure 4, Table 13, Figure 4) is doubtful. The form encountered by these authors 235 220 closely resembles Rhombodinium draco Gocht (Brosius und Graman, 1959, Table 6, Figures 1, 2) which is a dinoflagellate (Gocht, 1956). Deflandre (l.c.) notes the presence of small supporting spines in Vallacerta hortonii Hanna from the Upper Cretaceous of California. Such structures do not appear in the diagnoses and drawings of other authors. Our specimens do not possess supporting spines. 2. Vallacerta simplex Jousé (Plate I, 2). Zhuze (1949), Bot. mat. Otd. spor. rast. BIN AN SSSR, 6, 1—6, p. 77, Table 2, Figures 7—9; Glezer (1959), Inform. sb. VSEGEI, 10, p. 107, Figure 3. Skeleton composed of sculptured, apical pentagonal plate with almost straight, slightly convex_or concave sides, 13—28yuylong. Radial horns are usually small, rudimentary and rarely well developed, in which case they are of equal length. Sculpture consists of nodules, grooves and wrinkles. Distributioninthe USSR: Santonian-Campanian. Western Siberia: eastern slope of the Urals, Slavgorod suite, very rare to abundant (Nyais River, a tributary of the Severnaya Sosva River; Verkhotur'e area; Bol'shoi Aktai River). General distribution: Found only.in the USSR. Note: The species is linked by a series of transitional forms to the closely related Vallacerta hortonii Hanna. 3. Vallacerta tumidula Gleser (Plate I, 3—6). Glezer (1959), Inform. sb. VSEGEI, 10, p. 107, Figures 4, 5. Skeleton consists of an apical apparatus in form of pentagonal plate with bluntly rounded corners, almost straight or concave sides measuring 14—40 yu, a rounded central prominence of 9—25yu diameter and a narrow hyaline margin. Plate and prominence are covered by a network of nodules and ribs; occasionally a fine rib is evident at base of prominence. Radial horns 5—22ylong, often unequal, hollow, sometimes with rudimentary cavities. Distribution in the USSR: Santonian-Campanian. Western Siberia: eastern slope of the Urals, Slavgorod suite, very rare to common (Nes'-Yugan River, a left tributary of the Synya River; Verkhotur'e area). General distribution: Found only in the USSR. Note: This species differs from the closely related Vallacerta hortonii in the presence of a rounded prominence at the plate center. Order SIPHONOTESTALES Lemm. Lemmermann (1901), Ber. Dtsch. bot. Ges. 19, 1, p. 92. Skeleton, as a rule, composed of hollow tubular rods. 236 221 Key to the Families of the Order Siphonotestales I. Skeleton formed of elements of the apical apparatus; rudiments of basal Ping Ssumemmes present Trt. See Am. Cornuaceae (p. 237). II. Skeleton composed of basal and apical apparatus; latter sometimes not COvetp mE BES a a ys ie ew we we wo Dictyochaceae (p. 240). Family CORNUACEAE Gem. emend. Gleser Gemeinhardt (1930) Silicofl. in: Rabenhorst's Krypt.-Fl. 10, p. 77. Skeleton primitive, composed of 2— 4 apical rods, sometimes with rudiments of basal ring and supporting spines. Key to the Genera of the Family Cornuaceae 1. Skeleton simple, U- or Y-shaped......... Lyramula (p. 237). 2. Skeleton more complex; rods form a dome; supporting spines and a rudimeitary basal’ rine preseat 2 las Pe a Cornua (p. 238). Genus 2. Lyramula Hanna Hanna (1928), J. Paleont. 1, 4, p. 262; Deflandre (1950), Microscopie, 2, p. 49; Glezer (1959), Inform.sb. VSEGEI, 10, p. 108. Skeleton tubular, U- or Y-shaped, representing a primitive apical apparatus. Type: Lyramula furcula Hanna. Extinct marine genus. Key to Species of the Genus Lyramula i, Beletomh-shaped . ete fer) 4h << Bi eetaeredatad © L. simplex 1. fies eRe letpe Al Shapes, afi eh nek Tite Ee wlow bt sy edehe mee L. furcula 2. 1. Lyramula simplex Hanna (Plate II, 1, 2, 4). Hanna (1928), J. Paleontol. 1,4,p. 262, Table 41, Figure 6; Deflandre (1936), Actual. scient.ind. 335, p. 32, Figure 44; Deflandre (1940), C.r. Hebd. Séance Acad. Sci. 211, 21, Figures 5, 6; Deflandre (1950), Microscopie, 2, p. 61, Figures164,165; Zhuze (1951), Bot. mater. Otd. spor.rast. BIN AN SSSR, 7, p. 64, Table 6, Figure 3; Glezer (1959), Inform. sb. VSEGEI, 10, p. 109, Figures 9, 10; Krotov and Shibkova (1961), Mater. po geol. i polez. iskop. Urala, 9, Figures 2, 18. U-shaped skeleton composed of 2 hollow lateral rods, 30—123 yu long. Highly polymorphic species. Distribution inthe USSR: Santonian-Campanian. Western Siberia: eastern slope of the Urals and the Trans-Urals, Slavgorod suite, very rare 237 222 to frequent (Nes'-Yugan River, a left tributary of the Synya River; the basin of the Severnaya Sosva, Ust'-Man'ya village; Leplya and Nyais rivers; Loz'va River near Pristan' village; Ivdel', Serov and Verkhot'e areas); Kazakhstan: Kustanai Region, Kushmurun area, very rare. General distribution: Maestrichtian. North America (California, Moreno shales). 2. Lyramula furcula Hanna (Plate II, 3, 5—7). Hanna (1928), J. Paleontol. 1, 4, p. 262, Table 41, Figures 4, 5; Deflandre (1936), Actual. scient. ind. 335, p. 32, Figure 45; Deflandre (1940), C.r.Hebd. Séance Acad. Sci. 211, 21, Figures 1—3(?), 4; Deflandre (1950), Microscopie, 2, p. 61, Figures 163, 167—169 (?); Zhuze (1951), Bot. mater. Otd. spor. rast. BIN AN SSSR, 7, p. 64, Table 4, Figure 4; Glezer (1959), Inform. sb. VSEGEI, 10, p. 108, Figures 6—8; Krotov and Shibkova (1961), Mater. po geol. i polezn. iskop. Urala, 9, Figures 2, 17. — L. furcula var. minor Deflandre (1940), C.r. Hebd. Séance Acad. Sci. 211, 21, p. 509, Figure 10, 7—9 (?). — L. minor Deflandre (1950), Microscopie, 2, p. 62, Figures 170, 171—173 (?). Y-shaped skeleton composed of 2 hollow, curved lateral rods, often of unequal length, with a shorter outgrowth departing from their junction. Sculptured with hardly noticeable nodules. Skeletal contours are extremely variable. Length of the lateral rods 10—904y, of the outgrowth 3—18 uy. Distribution in the USSR:Santonian-Campanian. Western Siberia: eastern slope of the Urals, Slavgorod suite, very rare to abundant (Nes'- Yugan River, left tributary of the Synya River; the basin of the Severnaya Sosva, Ust'-Manya village; Leplya and Nyais rivers; the basin of the Loz'va River, Pristan' village; Pelym River; Ivdel' and Verkhot'e areas; Tynya River, Berezovo area); Kazakhstan: Kustanai Region, Kushmurun area, rare. Lower Paleocene. Western Siberia: eastern slope of the Urals, lower part of Talitsa suite, very rare (Makhnevo area). General distribution: Maestrichtian. North America (California, Moreno shales). Note: The new species Lyramula minor Deflandre was established on the basis of its shorter branches (42 —64 yu) in comparison with L. furcula Hanna (88—1004u). This is unjustified in my opinion because of the great variation of L. furcula Hanna. Genus 3. Cornua Schulz Schulz (1928), Bot. Arch. 21, 2, p. 285; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 77; Deflandre (1950), Microscopie, 2, p. 49; Glezer (1959), Inform. sb. VSEGEI, 10, p. 109. Hollow skeleton consists of apical apparatus and rudimentary basal ring. Apical apparatus consists of 3—4 lateral rods, forming a dome. Lateral rods end in the "terminal horns,'' which are rudiments of the basal ring. Terminal horns sometimes have supporting spines at their bases; accessory spines sometimes present. Hype: Cornuastznbiur e atari Schulz. Extinct marine genus. 238 Key to Species of the Genus Cornua RVArourtiateral rods 9 Sth were atl on Samaria oA Se Pa aC eer nd. Il. Three lateral rods. 1. Terminal horns, arising from adjacent lateral rods, almost parallel to ONS Sno er Ty SIRS RS AE PRS, PP OES C. trifureata 3. 2. Terminal horns, arising from adjacent lateral rods, arranged at acute angles to one another”... . 6. ss es SS. poretzkajyae 2:4 1. Cornua aculeifera Defl. (Plate III, 1). Deflandre (1940), C. r. Hebd. Séance Acad. Sci. 211, 23, p. 464, Figures 8, 9; Deflandre (1950), Microscopie, 2, p. 60, Figures 160 —162; Glezer (1959), Inform. sb. VSEGEI, 10, p.109, Figurell. — Cornua-like form of Dictyocha sp. indet. Deflandre (1944), C.r. Hebd. Séance Acad. pet, BIS 11,>p? 509, -Pioure 14. Four lateral rods end in more or less developed terminal horns and bear numerous accessory spines. Skeleton is highly variable (Deflandre, 43—65 yu; our specimen, 504). Distribution in the USSR: Santonian-Campanian. Western Siberia: eastern slope of the Urals, Slavgorod suite, very rare (Loz'va River, near village of Pristan'; Serov area). General distribution: Upper Cretaceous. North America (California, Moreno formation). 2. Cornua poretzkajae Gleser (Plate III, 2, 6). Glezer (1959), Inform.sb. VSEGEI, 10, p. 110, Figure 13. Three lateral are rods, 11—13.5yu1long. Terminal horns of each lateral rod aligned to form basal rods, which appear as branches, convex on the outside, 28—40 yu long, with sharp ends and a small central con- cavity. Terminal horns of adjacent lateral rods form acute angles to one another. Junction of lateral rods with basal rods is marked by one coarse supporting spine, about 5 uw long, directed to inside the dome. Height of skeleton 4—8 un. Distribution in the USSR. Santonian-Campanian. Western Siberia: eastern slope of the Urals, Slavgorod suite, rare (Leplya River; Verkhotur'e area). General distribution: Found only in the USSR. Note: This species differs from the closely related Cornua tri- furcata Schulz in the structure of the undeveloped basal ring: the aligned terminal horns form a single basal rod, while the adjacent basal rods are not parallel but form an acute angle with one another. 223 3. Cornua trifurcata Schulz (Plate ITI, 3—5). Schulz (1928), Bot. Arch. 21, 2, p. 285, Figure 83; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 59, Figures 157—159; Deflandre (1933), Bull. Soc. zool. Fr. 58, p. 1; Deflandre (1950), Microscopie, 2, p. 59, Figures 157—159; Glezer (1959), Inform. sb. VSEGEI, 10, p. 110, Figure 12. Three lateral rods are 8—13 y4 long. Terminal horns of each lateral rod, arranged atan angle of 90—120° to one another, are 11—21 yp long. Terminal horns arising from adjacent lateral rods are more or less parallel. Height of skeleton about 4 yu. 239 Distribution in the USSR: Santonian-Campanian. Western Siberia: eastern slope of the Urals, Slavgorod suite, very rare to abundant (Nes'- Yugan River, left tributary of the Synya River; the basin of the Severnaya Sosva, Ust'-Manya village; Leplya and Nyais rivers; Loz'va River near village of Pristan'; Serov and Verkhotur'e areas). General distribution: Senonian. Central Europe (Poland, Gulf of Danzig). Note: The spinules on the skeletal surface (Schulz, l.c.) were not found in the Ural form. Family DICTYOCHACEAE Lemm. Lemmermann (1901), Ber. Dtsch. bot.Ges. 19, 1, pp. 92—93. Skeleton usually is composed of basal and apical apparatus, the latter sometimes undeveloped. Basal ring is rounded, elliptical, triangular or polygonal with or without radial horns. Lateral rods arising from the basal ring either meet at one point or fuse terminally with one or several apical rods or the apical platform. Several apical rods sometimes form a rounded, triangular or polygonal apical ring with one or several, some- times numerous, apical windows. Supporting and accessory spines are often present. Key to the Genera of the Family Dictyochaceae I. Skeleton composed of basal and apical apparatus. 1. Apical apparatus consists of lateral or lateral and apical rods or of apical plate. A. Basal ring circular, oval, triangular or polygonal, always tubular; only in the triangular forms flattened areas sometimes present. a. Supporting spines, when Peo always located on basal ring. nes xn SOG wel. Shee Aan «.. » +» Dictyocha: (mi 24G)h. b. Supporting spines situated on Laseal rods near widened apical ro ee a ae Ln RSP eRe NSN Bee > Corbisema (p. 270) . B. Basal ring always elongated, bilaterally symmetrical, with flattened areas on lateral sides ..... Naviculopsis (p. 272) . See 2. Apical apparatus consists of lateral rods and an apical ring, simple or complex. A. Simple apical ring with one apical window. a. Basal ring with 10 or more corners; lateral rods very short with tendency to reduction; apical ring undulate ...... PT ere Irene 8. Paradictyocha (p. 296) ‘ b. Basal ring with 4—11 corners; lateral rods well developed; apical ring with straight sides ...7. Distephanus (p. 278). B. Apical ring with several apical windows. a. Apical apparatus strongly convex, hemispherical or spherical, its diameter roughly equal or greater than that of the basal Pilate dh atnadic oaks HP 6 ak ee Aaa 9. Cannopilus (p. 299) . 240 b. Apical apparatus slightly convex, its diameter less than that of basal ring; basal windows visible dorsally .......... thier Mitusoie. Sladiuea bos 7. Distephanus (p. 278) . II. No apical apparatus. ison Radial horns, if present, aligned... ...... 10. Mesocena (p. 302). 2. Radial horns arranged in2 rows ... .8. Paradictyocha (p. 296). Genus 4. Dictyocha Ehr. Ehrenberg (1839), Abhandl. Konig. Akad. Wiss., p. 128; Lemmermann (1901), Ber. Dtsch. Bot. Ges. 19, 1, p. 257; Schulz (1928), Bot. Arch. 21, 2, p. 234; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, puso. Basal ring is rounded, oval, triangular or polygonal and with or without radial horns; it is always tubular, but flattened areas are sometimes present only in triangular forms. Apical apparatus consists of one or several lateral or lateral and apical rods; the latter are sometimes un- developed. Supporting spines are situated on basal ring directly below the lateral rods or to their sides. Supporting spines sometimes are absent. Type: Dictyocha fibula Ehr. Living and extinct marine forms. Note: The genus Dictyocha was established in 1839 by Ehrenberg on the basis of fossil material from Oran, Algeria. Ehrenberg and, later, Kitzing (1849, 1865) placed in the new genus a morphological variety possessing ''a simple, univalve siliceous case shaped like a net or star." Later authors introduced marked changes in the definition of the genus Dictyocha Ehr. Hackel (1887), for example, placed some of the species of Dictyocha inthe genera Distephanus Stohr and Cannopilus Hack., and his views influenced the work of taxonomists such as Lemmer- mann (1901b), Schulz (1928) and Gemeinhardt (1930). The latter gives this definition of Dictyocha Ehr.: ''Skeleton composed of a basal ring above which rises a convex siliceous rod or a structure in the form of a hat or pyramid consisting of several siliceous rods" (Gemeinhardt, 1930, p. 35). Frenguelli (1940) and Deflandre (1950) made further modifications in the classification of the genus Dictyocha both by removing some of its species to the genera Naviculopsis Freng. and Corbisema Hanna and by returning to it species of Distephanus Stohr and most species of Cannopilus Hack. According to Frenguelli and Deflandre, the essential characteristic of the genus Dictyocha Ehr. is the position of the support- ing spines, which are more or less displaced from the location of the lateral rods. Deflandre points out, however, that this sign is not quite reliable since the supporting spines often do not develop. In such a case the genus must be identified on the basis of the general morphological similarity and phylogenetic affinities of the forms. In this work, the amplitude of the genus Dictyocha Ehr. has been adapted as defined by Hackel (1887) and interpreted in greater detail by Lemmermann (1901b), Schulz (1928) and Gemeinhardt (1930) with some changes introduced by Frenguelli and Deflandre. The latter modifications concern only species transferred to Naviculopsis Freng. 225 241 Key to Species of the Genus Dictyocha I. Basal ring triangular. 1. Lateral rods arise almost perpendicularly from plane of basal ring. Av Wecessory spines present eck. Sse G@ i -. D. spinosa 9): B.’ We aecessery spines’... belo J here ga. me ; D. elata 8 . 2. Lateral rods usually slope up from the inner margin of basal ring. A, Basal rile asyinmeirical’'. 2.7.88. 2578 J. D. elongata 7 B. Basal ring usually symmetrical. a. Middle part of basal rods are flattened and widened into a Srl aie POT 2s. 5, we Lee eee ees oe D. lamellifera 6 . b. No flattened areas on basal ring. Skeleton tubular. a. Basal ring with sharp or rounded apices . D. triacanthal . 8. Basal ring with bluntly truncated apices. * Each apex bears 2 rudimentary radial horns. + Skeleton thick, with strongly dentate walls : see tains ta dal. ise Seah O82 D. furcata 3 : ++ Skeleton leery thin with smooth walls ..... : ENALIGIOORS SHG | odes Reka doko el i ieee ane we; NGMAG al horns? °.! ss ios 6 tr SER D. archangelskiana 2 . II. Basal ring oval or circular. 1. Basal ring more or less oval. A. Apical apparatus consists of a single rod, radial horns absent, two basal windows present) «6. .0.06 ee le ee D. navicula 5 . B. Apical apparatus consists of apical and lateral rods; two radial horns and 4 basal windows present. a. Apical apparatus almost H-shaped; lateral rods curved, al- most perpendicular to plane of basal ring . D. transitoria 12 . b. Apical apparatus of different shape; lateral rods short, straight, arise from inner margin of basal ring; apical rod usually ‘widened: ; steeM.. aft. sricndate 1. B. Badal ring round or elliptical with alternating long and short facial lorns icon anbia Sedaris ibs. sated. os M. stellata 6. II. Radial horns absent. it bdealifingrpand er ellipticalissadA seco es Bias é M. circulus 5. 2. Basal ring triangular. A. Basal ring with round corners ..... . .M. oamaruensis 4. B. Basal ring with elongated, bluntly truncated corners. ..... OSS wpe eei: Auede pest Jfontidus s comets 22 MM) muticatasd:. oogs 1. Mesocena aff. apiculata (Schulz) Defl. (Plate XXVIII, 5; Plate XXIX, 9;) Plate XXXII, .7). Basal ring is an isosceles triangle with convex lateral sides, 40— 60y long and straight base, 25—50ulong. Radial horns are 4—7 wu, sometimes of unequal size: the horn departing from the apex is usually larger than the other two, which are often barely visible. Skeletal walls are clearly dentate. Canal is relatively narrow and distinct. Distribution in the USSR: Early Paleocene. Western Siberia: eastern slope of the Urals, Talitsa suite, very rare to frequent (Loz'va River near the village of Pristan'; Ivdel', Serov and Makhnevo areas). Late Eocene. Central Asia: Aral-Caspian area, basin of Irgiz River, upper part of Tas-Aran suite, very rare (Uzen'-Kairakty River). General distribution: Found in the USSR only. Note: In the form of the basal ring, specimens of the Paleocene of the eastern slope of the Urals resemble slightly M. apiculata (Schulz) Defl. from the Calvert formation of the Middle Miocene of California (Tynan, 1957, Table 1, Figure 10). They differ, however, in the almost regular symmetry of the basal ring and the unequal length of the radial horns. Specimens of the Late Eocene deposits of Uzen'-Kairakty River differ from the form described by Schulz (1928, p. 240, Figure 11) from Oamaru in possessing an isosceles basal ring and dentate skeletal walls. According to Schulz, the latter feature is characteristic of M. poly - morpha var. triangula (Ehr.) Lemm., which differs in the regular geometrical form of the skeleton. Schulz regards the regular geometrical form of the skeleton as one of the differences between M. oamaruensis Schulz s.l. and M. polymorpha Lemm. sens. lat. Deflandre (1932b, p. 499, Figures 34, 35) proposed that M. oamaruensis var. apiculata be considered as a separate species — M. apiculata (Schulz) Defl., which is characterized by the one-sided position of the radial horns. Deflandre's diagnosis does not fit the forms from the Paleogene deposits of Uzen'-Kairakty River or M. oamaruensis var. apiculata Schulz in the original drawing by Schulz. The scarcity of material prevents drawing any conclusion as to the taxonomic position of this form. 303 284 2. Mesocena elliptica Ehr. emend. Defl. (Plate XXIX, 1—7; Plate XXX, 1—5). Deflandre (1932), Bull. Soc. bot. Fr., 79, p. 497, Figures 21—29; Deflandre (1950), Microscopie, 2, Figures 75—80; Frenguelli (1940), Revista Mus. La Plata, Nuev. ser., 2, Secc. Paleontol. 7, Figure 9a—e; Zhuze (1955), Bot. Otd. spor. rast. BIN AN SSSR, 10, p. 80, Figures 8, 9; Proshkina- Lavrenko (1959), Tr. BIN AN SSSR, seriya 2, Spor. rast. 12, p. 156, Table 1, Figure 1 (?). — M. elliptica Ehrenberg (1854), Ber. Verhandl. Konig. Akad. Wiss., p. 208;Ehrenberg (1854), Mikrogeol., Table 20, Figure 44a. — M. triangula Ehrenberg (1840), Ber. Verhandl. Konig. Akad. Wiss., p. 208; Ehrenberg (1854), Mikrogeol., Table 22, Figure 41. — M. heptagona Ehrenberg (1843), Abhandl. Konig. Akad. Wiss., p. 417, Tables 1, 3, Figure 26; Ehrenberg (1854), Mikrogeol., Table 22, Figure 49. — M. octogona Ehrenberg (1843), Abhandl. Konig. Akad. Wiss., p. 417, Tables 1, 3, Figure 23. —?M. bisoctonaria Ehrenberg (1845), Ber. Verhandl. Konig. Akad. Wiss., p. 78; Ehrenberg (1854), Mikrogeol., Table 35A, gr. 18-B, Figure 10. — ?M. binonaria Ehrenberg (1845), Ber. Verhandl. Konig. Akad. Wiss., p. 78; Ehrenberg (1854), Mikrogeol., Table 35 A, gr. 18-B, Figure 9. — M. quadrangula Ehrenberg (1873), Abhandl. Konig. Akad. Wiss. Berlin, p. 145. — M. nonaria Ehrenberg, Ibid., p. 163. — M. diodon Ehrenberg (1844), Ber. Verhandl. Konig. Akad. Wiss., p. 84; Ehrenberg (1854), Mikrogeol., Table 33, gr. 15, Figure 18. — M. pentagona Hackel (1887), Voyage Challenger (Zool.), 18, 2, p. 1556. — M. crenulata var. diodon Lemmermann (1901), Ber. Dtsch. bot. Ges. 19, 1, p. 255, Table 10, Figure 1; Schulz (1928), Bot. Arch. 21, 2, p. 236, Figure la, b; Gemein- hardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 26, Figure 10a, b; Deflandre (1932), Bull. Soc. fr. Microsc., 1, 1, Figure 4. — M. crenu- lata var. elliptica Lemmermann (1901), Ber. Dtsch. bot. Ges. 19, 1, p. 255; Schulz (1928), Bot. Arch. 21, 2, p. 236, Figure 2; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 27, Figure 11. — M. polymorpha var. triangula Lemmermann (1901), Ber. Dtsch. bot. Ges. 19, 1; p. 255, Table 10, Figures 3, 4; Schulz (1928), Bot. Arch. 21, 2, p. 237, Figure 3a; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 28, Figure 12c; Deflandre (1932), Bull. Soc. fr. Microsce., 1, 1, Figure 5; Desikachary and Macheshwari (1956), J. Ind. Bot. Soc. 35, 3, p. 355, Text-figure 7, Table 13, Figure 1. — M. polymorpha var. quadrangula Lemmermann (1901), Ber. Dtsch. bot. Ges. 19, 1, p. 256, Table 10, Figures 5—7; Lemmermann (1903), Nord. Plankton, 2, 2, p. 26, Figure 89; Schulz (1928), Bot. Arch. 21, 2, p. 237, Figure 4a—c; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 29, Figure 13; Deflandre (1932), Bull. Soc. frang. microscopie, 1, 1, Figure 6; Cleve-Euler and Hessland (1948), Bull. Geol. Inst. Upsala, 32, p. 179, Table 16, Figure 79; Desikachary and Macheshwari (1956), J. Ind. Bot. Soc. 35, 3, p. 258, Text-figures 1, 3, 5, Table 13, Figure 2; In: Stratigrafiya mezozoya.. ., (1957), Table 135, Figure 15. —M. polymorpha var. pentagona Lemmermann (1901), Ber. Dtsch. bot. Ges. 19, 1, p. 256, Table 10, Figure 7; Schulz (1928), Bot. Arch. 21, 2, p. 238, Figure 5; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 30, Figure 14; Deflandre (1932), Bull. Soc. fr. Microsc., 1, 1, Figure 8; Ichikawa (1956), Sci. Rept. Kanazawa Univ. 5, 1, Text-figure 2. —M. polymorpha 304 var. hexagona Lemmermann (1901), Ber. Dtsch. bot. Ges. LOMA: p. 256; Schulz (1928), Bot. Arch. 21, 2, p. 238, Figure 6a (?); Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 30, Figure 15 (?); Deflandre (1932), Bull. Soc. fr. Microsc., 1, 1, Figure7(?); Ichikawa (1956), Sci. Rept. Kanazawa Univ. 5, 1, Text-figure 4. — M. polymorpha var. hexagona f. septenaria Schulz (1928), Bot. Arch. 21, 2, p. 238, Figure 7. — M. polymorpha var. hexagona f. octonaria Schulz (1928), Bot. Arch. 21, 2, p. 240, Figure 8a, b. — Lithocircus triangularis Stohr (1880), Palaeontogr. 26, 4, p. 121, Table 7, Figure 10. — Dictyocha triacantha var. hastata Lemm. sensu Cleve-Euler and Hessland (1948), Bull. Geol. Inst. Upsala, 32, p. 179, Table 14, Figure 78. Basal ring is of irregular geometrical form — rounded-square, irregu- larly elliptical, rounded-triangular or triangular, 25 —85 yu long and 20—60yu wide, with strongly convex sides. Radial horns numbering 2, 3 or 4 are often unequal in length, from 3 to 154, sometimes are absent. Skeletal walls are smooth or dentate. Distribution in the USSR: Eocene — Early Oligocene (?). Western Siberia: basin of Tura River, a tributary of the Tobol (Tyumen; Luchinkino village); basin of Tavda River, a tributary of the Tobol (villages of Kuznetsovo and Kamensko-Gusel'nikovo); Middle Ob area (Vakh River, Lar'yak village). Early Oligocene (?). Western Siberia: Taz peninsula, very rare to frequent (Khabirutta and En-Yakha rivers); Pelym River basin, Chegan suite, very rare to rare (Burmantovo village). Late Oligocene. Central Asia: Aral-Caspian area, Karagie suite, Mangyshlak peninsula. Early Miocene. European part: Crimea (Taman peninsula). General distribution: Eocene. Northern Europe (Sweden, Bay of Ahus). Late Oligocene — Early Miocene. South America (Lesser Antilles, Barbados). Aquitanian-Burdigalian stage. Southern Europe (Mor6én, Spain). Miocene. Southern Europe (Greece; Sicily, Italy); Central Europe (Hungary); Africa (Oran, Algeria); Asia (Nankoori, India); North America (Santa Monica, California). Neo- gene (?). North America (Santa Maria; Redondo; Richmond; Maryland, etc.). Note: Skeletons of this species from the Paleogene of Western Siberia and Mangyshlak are distinguished by a wide variation in the contour of the basal ring, although the number of their radial horns never exceeds 4. Some of these specimens resemble those described by Schulz (1928, Figures 1b, 2, 3a) from the Neogene of Richmond and Nottingham (North America) and Zante (Greece). Deflandre (1932b) united in one species Mesocena elliptica Ehr. a number of forms, described by Ehrenberg (l.c.) as numerous separate species of the genus Mesocena and treated by Lemmermann (1901b) and other taxonomists as varieties of two species: M. polymorpha Lemm. and M. crenulata Ehr. Deflandre's work lacks a diagnosis or synonymy of M. elliptica Ehr., and only mentions a few species established by Ehrenberg and regarded by Lemmermann (1901b) as varieties of M. polymorpha Lemm. Deflandre stresses the poly- morphism of the species, noting that it has a variety of forms bearing a different number of radial horns (from 2 to 9). This feature is shown in illustrations, but data are not given on the distribution of the species in this work. 285 305 286 3. Mesocena muticata Gleser (Plate XXVIII, 4). Glezer (1964), Novosti sist. nizsh. rast., p. 58, Table 2, Figure 11. Basal ring is more or less regular equilateral triangle with slightly concave sides, 75—86yu long, and somewhat produced, bluntly truncated corners. Skeletal walls are dentate. Distribution in the USSR: Early Oligocene (?). European part: left bank of the Dnieper, north of Nizhne-Dneprovskii Uzel' station, very rare. General distribution: Found in the USSR only. Note: Differs from M. oamaruensis Schulz in the elongated, bluntly truncated corners, which are somewhat reminiscent of Dictyocha archangelskiana (Schulz) Gleser; but the marked difference includes total absence of apical apparatus and supporting spines. 4. Mesocena oamaruensis Schulz (Plate XXVIII, 3). Schulz (1928), Bot. Arch. 21, 2, p. 240, Figure 10a, b; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 34, Figure 20; Deflandre (1932), Bull. Soc. fr. Microsc., 1, 1, Figure 11. Basal ring is an equilateral triangle with straight or concave sides, 66—70u long, and round corners. Distribution in the USSR: Late Eocene. Central Asia: Aral- Caspian area, basin of the Irgiz, upper part of Tas-Aran suite, very rare (Uzen'-Kairakty River). Early Oligocene (?). European part: left bank of the Dnieper, north of Nizhne-Dneprovskii Uzel station, Kharkov (?) suite, very rare. General distribution: Late Eocene. North America (California), Late Eocene or Early Oligocene. Australia (Oamaru, New Zealand). 5. Mesocena circulus Ehr. (Plate XXIX, 8). Ehrenberg (1840), Ber. Verhandl. Konig. Akad. Wiss., p. 208; Ehren- berg (1854), Mikrogeol., Table 19, Figure 44; Lemmermann (1901), Ber. Dtsch. bot. Ges. 19, 1, p. 257, Schulz (1928), Bot. Arch. 21, 2, p. 242; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 33, Figure 18. Skeleton consists of round or oval basal ring, 72 u long, 60 yu wide, with dentate walls. Distribution in the USSR: Sea of Japan (Peter the Great Bay). FOSSILS. Eocene. European part: Volga area (Kuznetsk). Late Eocene. Western Siberia: Taz peninsula, very rare. Late Eocene — Early Oligocene (?). Eastern slope of the Urals, lower part of Chegan suite, very rare (Ivdel' area). General distribution: Early Eocene. Western Europe (Denmark, Mors Island). Late Eocene — Early Miocene. South America (Lesser Antilles, Barbados). Miocene. Southern Europe (Italy; Greece); Asia (Sendai, Honshu Island, Japan). Note: Similar in dimensions to specimens described by Ehrenberg (1854) from the Neogene deposits of Greece, but differs in the oval form. Larger than skeletons found by Schulz (l.c.) in the deposits of Kuznetsk and by Lemmermann (1. c.) in Greece and Italy. Gemeinhardt (l.c.) regards the establishment of M. circulus Ehr. as superfluous in view of its close similarity to M. crenulata Ehr. It should be remembered that 306 Ehrenberg described the latter species after M. circulus Ehr.; more- over, no drawing was published. Deflandre (1932b) notes that skeletons analogous to the schematic drawing in Schulz (l.c.) are fairly common in the diatomites of Sendai, Japan. He does not believe that these are silicoflagellates. The morphology of the skeletons encountered in the lower part of the Chegan suite of the eastern slope of the Urals indicates without doubt that these belong to the silicoflagellates. 6. Mesocena stellata Hack. (Plate XXVIII, 2). Hackel (1887), Voyage Challenger (Zool.), 18, 2, p. 1557, Table 101, Figure 9. — M. circulus var. stellata Lemmermann (1901), Ber. Dtsch. bot. Ges. 19, 1, p. 257; Gemeinhardt (1930), Silicofl. In: Rabenhorst's Krypt.-Fl. 10, p. 34. Basal ring is circular or oval, 42—45y long, 37—40u wide. Radial horns, situated in one plane, number 12—14; longer horns measuring 9—10 yu alternate with shorter ones, 4—5uy long. Distribution in the USSR: Neogene. Far East: Sakhalin (Shmidt peninsula, basin of the Kongi and Tumi rivers, very rare). General distribution: Pacific Ocean (central part). Note: Alternation of long and short radial horns is reminiscent of the skeletons of M. stellata Hack. we described from the Pacific Ocean, but differs from it in the slightly larger size of the basal ring and the smaller amount of radial horns (according to Hackel, the respective figures are 30yu and 16 horns). Deflandre (1932b) assumed that M. circulus var. stellata (Hack.) Lemm. (= M. stellata Hack.) should be removed from the genus Mesocena Ehr. This hypothesis can be confirmed or rejected after more material becomes available. 307 Az Ses ie oe IN ATA PLATE I 1—Vallacerta hortonii Hanna. Eastern slope of the Urals, Pristan' village on Loz‘va River (well 268, 83.8—88.0 m), Slavgorod suite, Santonian-Campanian; 2—V. simplex Jousé. Eastern slope of the Urals, Bol'shoi Aktai River, Upper Cretaceous (Zhuze, 1949a); 3—6 —V. tumidula Gleser. Eastern slope of the Urals, Verkhotur'e area (well 13, 24.9 m), Slavgorod suite, Santonian-Campanian; 7—V. hannai Defl. California, Moreno formation, Upper Cretaceous (Deflandre, 1950). 308 PLATE II 1,2,4—Lyramula simplex Hanna. Eastern slope of the Urals, Nes'-Yugan River, Santonian-Campanian; 3,5—7 — L. furcula Hanna. Eastern slope of the Urals, Verkhotur'e area (well 13, 24.9 m), Slavgorod suite, Santonian-Campanian. 309 eee 1—Cornua aculeifera Defl. Eastern slope of the Urals, Serov area (well 771, 120,6 m), Slavgorod suite, Santonian-Campanian; 2,6—C. poretzkajae Gleser (2—view from side, 6 — from below). Eastern slope of the Urals, Verkhotur'e area (well 13, 25.2 m), Slavgorod suite, Santonian-Campanian; 3-5 —C. trifurcata Schulz. Eastern slope of the Urals, Verkhotur’e area (well 13, 26.0 m), Slavgorod suite, Santonian-Campanian. PLATE Ill 310 PLATE IV 1—6—Dictyocha triacantha Ehr. var. triacantha f, triacantha (2—4, 6 — view from above, 1, 5—from below); 1—basin of Irgiz River, right bank of the Uzen'-Kairakty, upper part of Tas-Aran suite, Late Eocene; 2— Dnepropetrovsk (well 12, 35.7—39.0 m), Kharkov (?) suite; 3—5 — eastern slope of the Urals, Serov area (well 771, 15.5 m), lower part of Talitsa suite, Early Paleocene; 4—eastern slope of the Urals, Ivdel' area (well 130, 137.3 m), Irbit suite, Middle Eocene (?); 6 — eastern slope of the Urals, Makhnevo area (well 1482, 34.8 m), lower part of Talitsa suite, Early Paleocene. 311 PLATE V 1—4 —Dictyocha triacantha Eh, var, triacantha f. triacantha (view from below); 1—basin of Irgiz River, right bank of Uzen'-Kairakty, upper part of Tas-Aran suite, Late Eocene; 2—Middle Volga area, Ul'yanovsk Region, Sengilei, Granoe Ukho quarry, Kamyshin bed; 3,4 —Oamaru, New Zealand, - Late Eocene or Early Oligocene. 5,6,8,10—D. t. var. flexuosa (Stradner) Gleser (view from below): 5 — Ukrainian SSR, Krasnyi Oskol village, Kharkov (?) suite; 6, 8 — basin of Irgiz River, right bank of Uzen'-Kairakty, upper part of Tas-Aran suite, Late Eocene; 10 —Mangyshlak peninsula, Karagie suite, Late Oligocene. 7,9—D.t. var. triacantha f. minor Schulz (view from below): 7—Oamaru, New Zealand, Late Eocene or Early Oligocene; 9—Middle Volga area, Ul'yanovsk Region, Sengilei, Granoe Ukho quarry, Kamyshin strata, Early Eocene. 312 PLATE VI 1—Dictyocha triacantha var. apiculata f. late-radiata Schulz (view from below), Eastern slope of the Urals, Loz'va River, Pristan' village (well 268, 88.0—96.8 m), Slavgorod suite, Santonian- Campanian; 2—4 —D.t. var. apiculata f. minor Schulz, Eastern slope of the Urals, Ivdel' area (well 130, 74.5 m), Irbit suite, Late Eocene; 5—D.t. var. apiculata Lemm. f. apiculata. Eastern slope of the Urals, Makhnevo area (well 1482, 34.8 m), lower part of Talitsa suite, Early Paleocene; 6—8 — D. t. var. hastata Lemm. (6,8—view from above, 7—from below); 6,7 — eastern slope of the Urals, Makhnevo area (well 1482, 34.8 m), lower part of Talitsa suite, Early Paleocene; 8 — Middle Volga area, Ul'yanovsk Region, Sengilei, Lower Syzran bed, Early Paleocene. 313 PLATE Vil 1—8 —Dictyocha triacantha var. hastata Lemm.; 1,4, 5, 8—view from below, 2,3, 6, 7—from above: 1 —basin of Irgiz River, right bank of Uzen'-Kairakty, upper part of Tas-Aran suite, Late Eocene; 2 —eastern slope of the Urals, Ivdel' area (well 139, 74.5 m), Irbit suite, Late Eocene; 3, 5—8 — eastern slope of the Urals, Makhnevo area (well 1482, 34.8 m), lower part of Talitsa suite, Early Paleocene; 4—Oamaru, New Zealand, Late Eocene or Early Oligocene. 314 PLATE VIII 1,2—Dictyocha triacantha var. inermis Lemm. f. inermis (view from below); 1 — eastern slope of the Urals, Makhnevo area (well 1482, 34.8 m), lower part of Talitsa suite, Early Paleocene; 2 — eastern slope of the Urals, Verkhotur'e area (well 13, 25.2 m), Slavgorod suite, Santonian-Campanian. 3—5 —D. t. var. inermis f. minor Gleser (3, 5— view from below, 4—from above). Eastern slope of the Urals, Ivdel' area (well 564, 172.7 m), lower part of Talitsa suite, Early Paleocene. 6, 7—D. archangelskiana (Schulz) Gleser (6 — view from above, 7 — from below); 6 —Oamaru, New Zealand, Late Eocene or Early Oligocene; 7— eastern slope of the Urals, Ivdel' area (well 564, 163.0 m), lower part of Talitsa suite, Early Paleocene. 315 PLATE IX 1—Dictyocha ausonia Defl. Sakhalin, western coast of Shmidt peninsula, Mayam-Raf suite, Neogene; 2—D. bimucronata (Defl.) Tsumura. Kharkov Region, Staroverovka village, Kharkov (?) suite, Early Oligocene (?); 3—D. aff. fibula var. rhombus (Hack.) Lemm, (view from below). Basin of Irgiz River, right bank of Uzen'-Kairakty, upper part of Tas-Aran suite, Late Eocene; 4, 5—Dictyocha navicula Ehr. (4—view from below, 5— from above); 4— eastern slope of the Urals, Ivdel’ area (well 564, 51.0 m), Serov suite, Early Eocene; 5—Middle Volga area, Sengilei, Granoe Ukho quarry, Kamyshin bed, Early Eocene. 6—Phyllodictyocha schulzii Defl. (view from below). Lesser Antilles, Barbados Island, Late Eocene— Early Miocene; 7—Corbisema geometrica Hanna, California, Moreno formation, Upper Cretaceous (Deflandre, 1950). 5698 316 PLATE X 1,4—Dictyocha elata Gleser var. elata (1—view from below, 4— from above), Eastern slope of the Urals, Serov area (well 771, 15.5 m), Irbit suite, Late Eocene; 2,3,5—D. elata var. media Gleser f. media (2,3 —view from below, 5—from above). Southern part of Taz peninsula, right bank of En- Yakha River, Early Oligocene (?); 6—8 —D. spinosa (Defl.) Gleser (view from above): 6, 8 — basin of Irgiz River, right bank of Uzen'-Kairakty , upper part of Tas-Aran suite, Late Eocene; 7 — southern part of Taz peninsula, right bank of En-Yakha River, Early Oligocene (?). 9—D. elata var. media f. reducta Gleser (view from below). Southern part of Taz peninsula, right bank of En- Yakha River, Early Oligocene (?); 10—D. lamellifera var. hastata Gleser (view from below), Eastern slope of the Urals, Seroy area (well 762, 27.0 m), Serov suite, Early Eocene; 12—D. hexacantha Schulz (view from above). Left bank of Dnieper, Nizhne-Dneprovskii Uzel station (well 12, 32.0—35.7 m), Kharkov (?) suite, Early Oligocene (?); 11,138,14—D. lamellifera Gleser var. lamellifera (13 —view from side, detail; 11, 14 —from below): 11 —skeleton without supporting spines; 14 —skeleton with supporting spines. Eastern slope of the Urals, Ivdel' area (well 564, 75.5 m), Serov suite, Early Eocene. 15—-17—D. lamellifera var. constricta Gleser (15,17 —view from below, 16 — from above); 15—Middle Volga area, Ul'yanovsk Region, Sengilei, Granoe Ukho quarry, Kamyshin bed; 16, 17 —eastern slope of the Urals, Ivdel’ area (well 564, 18.0 m), Serov suite, Early Eocene. 317 PLATE XI 1—7 —Dictyocha elongata Gleser(1,3—6—view from above, 2 — from below, 7 — from side). Eastern slope of the Urals, Serov area (well 762, 27.0 m), Serov suite, Early Eocene. 8,10—13 —D, frenguellii var. carentis Gleser f. carentis(8,11—view from side, 10 — from above, 12, 13 — from below): 8,11, 12 — eastern slope of the Urals, Ivdel' area (well 130, 55.0—60.4 m), Irbit suite, Late Eocene; 10,13 —Malyi Atlym village (well 6-k, 320 m), Lyulimvor suite, Late Eocene. 9—D. frenguel- lii Defl. var. frenguellii, view from above. Malyi Atlym village (well 6-k, 320.0 m), Lyulimvor suite, Late Eocene. 14—16—D. frenguellii var. carentis f. incerta Gleser (14 — view from side, 15— from above, 16—from below). Eastern slope of the Urals, Ivdel' area (well 130, 55.0—60.4 m), Irbit suite, Late Eocene. 17—20—D. rotundata Jousé var. rotundata (17, 18 — view from side, 19— from below, 20—from above). Eastern slope of the Urals, Ivdel' area (well 130, 16.0 m), Chegan suite, Late Eocene —Early Oligocene (?). 318 PLATE XII 1—6, 11, 12—Dictyocha rotundata var. secta Gleser(1,2,4 — view from below; 3, 5, 6 — from above; 11,12 — from side). Middle Ob area, Parabel‘ and Chuzik section (well 10-k, 155.5—162.7 m), Chegan suite, Late Eocene—Early Oligocene (?). 7—10—D. transitoria Defl. (7,9—view from below; 8,10—from above). Eastern slope of the Urals, Ivdel' area (well 130, 38.7 m), Irbit suite, Late Eocene. 13,16—D. deflandrei Freng. var. deflandrei (13 — view from below, 16 — from above); 13 —Middle Volga area, Ul'yanovsk Region, Sengilei, Granoe Ukho quarry, Kamyshin bed; 16 — eastern slope of the Urals, Alapaevsk area (well 31, 6.0m), Serov suite, Early Eocene. 14,15—D. d. var. completa Gleser f. completa (14—view from below, 15 —from above); 14 — eastern slope of the Urals, Ivdel" area (well 130, 31.8 m), Irbit suite, Late Eocene; 15— eastern slope of the Urals, Ivdel' area (well 130, 16.0 m), Chegan suite, Late Eocene— Early Oligocene (?). 17—19—D. d. var. completa f. producta Gleser (17,18 — view from below, 19—from above). Eastern slope of the Urals, Ivdel' area (well 130, 16.0 m), Chegan suite, Late Eocene—Early Oligocene (?). 20-23 — D. deflandrei var. bicornuta Gleser (20—22 —view from above, 23 — from below). Eastern slope of the Urals, Ivdel' area (well 130, 16.0 m), Chegan suite, Late Eocene—Early Oligocene (?). Bb PLATE XIII 1—5—Dictyocha obliqua Gleser(1—3, 5 —view from below, 4— from above). Eastern slope of the Urals, Ivdel' area (well 130, 16.0 m), Chegan suite, Late Eocene—Early Oligocene (?). 6—9—D. fibula Ehr. var. fibula f. fibula (view from below): 6—Middle Ob area, Parabel' and Chuzik section (well 7-k, 177.25—185.85 m), Lyulimvor suite, Late Eocene; 7 — eastern slope of the Urals, Ivdel' area (well 130, 31.8 m), Irbit suite, Late Eocene; 8, 9—Ivdel’ area (well 130, 16.0 m), Chegan suite, Late Eocene— Early Oligocene (?). 320 PLATE XIV 1-9 —Dictyocha fibula Ehr. var. fibula f. fibula (1,2,4, 5,8 —view from above; 3, 6,7, a from below); 1,2—Sakhalin, Kongi and Tumi rivers, Diatom suite, Neogene; 3 — plankton of Pacific Ocean; 4 —Dnepropetrovsk (well 12, 32.0—35.7 m), Kharkov (?) suite; 5—Sakhalin, Shmidt peninsula, Kongi River and Lake Machigar, Diatom suite, Neogene; 6 —Leningrad Region, Mga River, Quaternary intermoraine deposits; 7 —South America, Peru, Neogene (?); 8 —New Zealand, Oamaru, Late Eocene or Early Oligocene; 9 — eastern slope of the Urals, Ivdel' area (well 130, 31.8 m), Irbit suite, Late Eocene. 321 PLATE XV 1—3—Dictyocha fibula var. pentagona Schulz (1,2—view from above, 3— from below): 1— Middle Ob area, Parabel' and Chuzik section (well 10-k, 155,5—162.7 m), Chegan suite, Late Eocene—Early Oligocene(?); 2,3 —northern Sakhalin, eastern coast of Shmidt peninsula, Diatom suite, Neogene. 4,5,7,9—D. fibula var. fibula f. rhombica Schulz (4,7, 9—view from below; 5 — from above): 4—Italy, Mondaino, Neogene(?); 5,7 —Middle Volga area, Sengilei, Granoe Ukho quarry, Kamyshin bed; 9— basin of Irgiz River, right bank of Uzen'-Kairakty, upper part of Tas-Aran suite, Late Eocene. 6—D. fibula var, fibula f. eocaenica Krotov (view from below). Eastern slope of the Urals, Ivdel' area (well 564, 4.3 m), Serov suite, Early Eocene. 8—D. fibula var. messanensis (Hack.) Lemm. (view from above). Pacific Ocean near the southern coast of Kamchatka, bottom sediments. 322 PLATE XVI 1—Naviculopsis robusta Defl. (view from above). Eastern slope of the Urals, Serov area (well 762, 27.0 m), Serov suite, Early Eocene. 2—5—N. biapiculata (Lemm.) Freng. var. biapic ulata (2,3,5—view from above, 4— from below): 2,5 —eastern slope of the Urals, Ivdel' area (well 130, 31.8 m), Irbit suite, Late Eocene; 3 — Middle Ob area, Vasyugan section (well 3-k, 232.35—239.85 m), Lyulimvor suite, Late Eocene; 4—Denmark, Mors Island, Early Eocene. 6—8 —N. b. var. minor (Schulz) Gleser (6 — view from below, 7, 8 — from side): 6 —Middle Ob area, Ul'yanovsk Region, Sengilei, Granoe Ukho quarry, Kamyshin bed; 7, 8 — eastern slope of the Urals, Ivdel' area (well 130, 31.8 m), Irbit suite, Late Eocene. 323 UY PLATE XVII 1—3,6—Naviculopsis biapiculata var. minor (Schulz) Gleser (view from above); 1, 6 — eastern slope of the Urals, Ivdel' area (well 130, 31.3 m), Irbit suite, Late Eocene; 2 — Dnepropetrovsk Region (well 4741, 58.0 m), Kharkov (?) suite; 3 — basin of Irgiz River, right bank of Uzen'-Kairakty, upper part of Tas-Aran suite, Late Eocene. 4—N. biapiculata var. constricta (Schulz) Gleser (view from above). Basin of Irgiz River, right bank of Uzen'-Kairakty, upper part of Tas-Aran suite, Late Eocene. 5—N. foliacea Defl. (view from above). Lesser Antilles, Barbados Island, Late Eocene— Early Miocene. 7—N. trispinosa (Schulz) Gleser (view from side). Oamaru, New Zealand, Late Eocene or Early Oligocene (Gemeinhardt, 1930), 8—11—Distephanus antiquus Gleser (8 —view from side, 9— from below, 10,11 — from above). Southern part of Taz peninsula, right bank of En-Yakha River; Early Oligocene (?). 324 PLATE XVIII 1—11—Distephanus crux (Ehr.) Hack. var. crux. (1,10—view from below; 2,3, 5, 6, 8, 9, 11 — from above; 4, 7— from side); 1,5—8 — Kamchatka, Napana River, Kakertok suite, Neogene; 2,4 — Sakhalin, Kongi and Tumi rivers, Neogene; 3, 9— Sakhalin, Shmidt peninsula, Machigar section, lower part of Diatom suite, Neogene; 11 —Mangyshlak peninsula, Karagie suite, Late Oligocene. 325 PLATE XIX 1—6 — Distephanus crux (Ehr.) Hack. var. crux (1,2,3,5—view from above; 4, 6 — from side); 1,4 —Japan, Onnagawa formation, Middle Miocene; 2, 3—basin of Irgiz River, Uzen'-Kairakty, upper part of Tas-Aran suite, Late Eocene; 5, 6 — western part of Northern Caucasus, Shibik River, Early Miocene. 7—9-—D. speculum (Ehr.) Hack. var. speculum (7—double skeleton, side view; 8— view from above, 9—from below); 7 —Kiel Bay, plankton (Gemeinhardt, 1930); 8—New Zealand, Oamaru, Eocene or Early Oligocene; 9 — Western Siberia, Middle Ob area, basin of Vasyugan River (well 3-k, 193,.9— 201.9 m), Chegan suite, Late Eocene—Early Oligocene (?). 10—D. stauracanthus (Ehr.) Hack. North America, Santa Monica, Middle— Late Miocene (Schulz, 1928). 326 PLATE XX 1-11 —Distephanus speculum (Ehr.) Hack. var. speculum (1,2,4, 6, 8-10 — view from above; 3,7,11—from below; 5—side view from above): 1—3, 6,7 —Sakhalin, eastern coast of Shmidt peninsula, Neogene; 4—southern Sakhalin, Lyutoga River, Maruyama suite, Neogene; 5 — Sakhalin, northern coast of Shmidt peninsula, Machigar section, Diatom suite, Neogene; 8 —northern Sakhalin, basin of Kongi and Tumi rivers, Neogene; 9 — Leningrad Region, Otradnoe station (well 700, 13.0—13.5 m), Mga Quater- nary clays; 10-11 —Mangyshlak peninsula, Karagie suite, Late Oligocene. 327 PLATE XXI 1—5 —Distephanus speculum var. pentagonus Lemm. (1,2,4,5—view from above, 3 — from below): 1—basin of Irgiz River, Uzen'-Kairakty, upper part of Tas- Aran suite, Late Eocene; 2— Western Siberia, Taz peninsula, right bank of En-Yakha River, Early Oligocene (?); 3—5 — northern Sakhalin, northern coast of Shmidt peninsula, Machigar section, Diatom suite, Neogene. 6—D. speculum var. septenarius (Ehr.) Jorg. (view from above). Kamchatka, Ust'-Kamchatsk area, Neogene. 7—8 — D. octo- narius var. polyactis (Jorg.) Gleser (7 —view from above, slightly to the side; 8 — from below). Kamchatka, Ust'-Kamchatsk area, Neogene. 9—D. speculum var. regularis Lemm (view from above). Plankton (Gemeinhardt, 1930). 328 PLATE XXII 1-—5—Distephanus speculum var. cannopiloides (Pr.-Lavr.) Gleser (1,2 — view from below; 3,5 —from above; 4 — from above and slightly to the side); 1 —basin of Irgiz River, right bank of Uzen'- Kairakty, upper part of Tas- Aran suite, Late Eocene; 2—5 — northern Sakhalin, northern coast of Shmidt peninsula, Machigar section, upper part of Diatom suite. 329 330 PLATE XXIV 1—5—Distephanus speculum var. cannopiloides (Pr.-Lavr.) Gleser (1, 3,4 — view from below; 2,5—from above). Sakhalin, northern coast of Shmidt peninsula, Machigar section, lower part of Diatom suite. 6—Nothyocha insolita Defl. Greece, Tortonian (Deflandre, 1952). 7—11 — Paradictyocha polyactis Freng. f. polyactis (7—view from above; 9—from below; 8, 10,11 —structural details, side view): 7—northern Sakhalin, basin of Kongi and Tumi rivers, Neogene; 8—11 —northern Sakhalin, northern coast of Shmidt peninsula, Machigar section, middle part of Diatom suite, Neogene. 331 PLATE XXV 1, 3-8,10 —Distephanus japonicus f. pseudofibula (Schulz) Gleser (1, 3, 5, 6, 7 —view from above; 4, 8, 10—from below). Southern Sakhalin, Pervomaiskoe area, Maruyama suite, Neogene. 2,9—D. japonicus (Defl.) Gleser f. japonicus (view from above). Northern Sakhalin, Troptun and Longi rivers, Neogene. 11—D. octonarius var. cyrtoides (Hack.) Gleser (view from above). Pacific Ocean near southern coast of Kamchatka, plankton. 5698 332 PLATE XXVI 333 PLATE XXVII 1—4 —Cannopilus hemisphaericus (Ehr.) Hack. (1, 3—view from above, 2— from side, 4— from below): 1—3 — eastern slope of the Urals, Ivdel' area (well 130, 55.0—60.4 m), Irbit suite, Late Eocene; 4 —northern Sakhalin, northern coast of Shmidt peninsula, Machigar section, lower part of Diatom suite. 5—C. sphaericus Gem. (view from side). Hungary, Miocene (Frenguelli, 1940). 334 3 PLATE XXVIII 1—Paradictyocha polyactis f. mesocenoidea (Defl.) Freng. Northern Sakhalin, basin of Kongi and Tumi rivers, Neogene; 2 — Mesocena stellata Hack. Northern Sakhalin, basin of Kongi and Tumi rivers, Neogene; 3—M. oamaruensis Schulz. Dnepropetrovsk Region (well 4741, 58.0 m), Kharkov (?) suite, Early Oligocene (?); 4—M. muticata Gleser. Dnepropetrovsk, left bank of the Dnieper (well 12, 35.7—39.0 m), Kharkov (2) suite, Early Oligocene (?); 5—M. aff. apicu lata (Schulz) Defl. Eastern slope of the Urals, Makhnevo area (well 1482, 43.3 m), lower part of Talitsa suite, Early Paleocene. 345 f : 1 3 4 80A PLATE XXIx 1—7—Mesocena elliptica Ehr. emend. Defl. Southern part of Taz peninsula, right bank of En- Yakha River, Early Oligocene (?); 8—M. circulus Ehr. Eastern slope of the Urals, Ivdel‘ area (well130, 16.0 m), Chegan suite, Late Eocene—Early Oligocene (?); 9—M. aff. apiculata (Schulz) Defl. Basin of Irgiz River, Uzen'-Kairakty, upper part of Tas-Aran suite, Late Eocene. 336 2 Oo PLATE XXX 1-5 — Mesocena elliptica Ehr, emend Defl. Mangyshlak peninsula, Karagan suite, Late Oligocene. 337 PLATE XXxI 1—Vallacerta hortonii Hanna. Eastern slope of the Urals, Pristan’ village on Loz'va River (well 268, 83.8—88.0 m), Slavgorod suite, Santonian-Campanian. 2,3—Dictyocha triacantha Ehr. var. triacantha f. triacantha (view from side). Eastern slope of the Urals, Ivdel' area (well 564, 172.7 m), lower part of Talitsa suite, Early Paleocene. 4—6 —D. t. var. apiculata f. minor Schulz (view from above); 4, 5 — eastern slope of the Urals, Makhnevo area (well 1482, 43.3 m), lower part of Talitsa suite, Early Paleocene; 6 —southern part of Taz peninsula, Arka-Tab-Yakha River, Late Eocene. 7—D. t. var. inermis f. minor Gleser (view from below). Eastern slope of the Urals, Ivdel' area (well 564, 172.7 m), lower part of Talitsa suite, Early Paleocene. 8,9—D. t. var. hastata Lemm. (view from below). Eastern slope of the Urals, Ivdel' area (well 564, 172.7 m), lower part of Talitsa suite, Early Paleocene. 338 PLATE XXXII 1—Dictyocha triacantha var. inermis Lemm, f. inermis (view from above). Eastern slope of the Urals, Makhnevo area (well 1482, 34.8 m), lower part of Talitsa suite, Early Paleocene; 2—D. lamel- lifera var. constricta Gleser (view from above). Eastern slope of the Urals, Ivdel' area (well 564, 18.0 m), Serov suite, Early Eocene; 3—D. lamellifera Gleser var. lamellifera (view from above). Eastern slope of the Urals, Ivdel' area (well 564, 75.5 m), Serov suite, Early Eocene; 4—D. deflandrei Freng. var. deflandrei (view from above). Middle Volga area, Ul'yanovsk Region, Sengilei, Granoe Ukho quarry, Kamyshin bed; 5—D. fibula var. fibula f, eocaenica Krotrv (view from below). Eastern slope of the Urals, Ivdel' area (well 564, 51.0 m), Serov suite, Early Eocene; 6—D. furcata Jousé (view from below). Eastern slope of the Urals, Makhnevo area (well 547, 33.0 m), lower part of Talitsa suite, Early Paleocene. 339 PLATE XXXIII 1,2—Dictyocha frenguellivar. carentis Gleser f. carentis (1—view from below, 2— from side). Eastern slope of the Urals, Ivdel' area (well 130, 128.7 m), Irbit suite, Middle (?) Eocene; 3—6 — Naviculopsis robusta Delf. (3,5,6—view from above, 4— from side). 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(Mesocena) 282, 283, Plate XXVIII, 5; XXIX, 9; XXXIII, 7 apiculata Freng. (Paradictyocha) 279 archangelskiana (Schulz) Freng. (Corbi- sema) 232 archangelskiana (Schulz) Gleser (Dictyo- cha) 225, 232, 233, 253, 285, Plate VIII, 6,7 asteroides Hack. (Distephanus) 267 ausonia Defl. (Dictyocha) 226, 252, Plate IX, 1 biapiculata (Lemm.) Defl. (Dictyocha) 253, 204, 250 — f. eocaenica Krotov 254 biapiculata Lemm. (Dictyocha ?) 255, 256, 257, 258 biapiculata (Lemm.) Freng. (Naviculop- sis) 235, 254, 259, 257; 258, 259 — f. triacantha Freng. 235 var. biapiculata 255, ra6a. XVI, 2—5 var. constricta (Schulz) Gleser, 257, Plate XVII, 4 — var. minor (Schulz) Gleser 256, Plate. XVI, 6—8; XVII, 1—8, 6 bimucronata Defl. (Corbisema) 233, 253 bimucronata (Defl.) Tsumura (Dictyocha) 225, 233; “Plate Eke binoculus (Ehr.) Lemm. (Cannopilus) 270, 271 — var. diommata (Ehr.) Lemm. 270 binoculus Ehr. (Dictyocha) 269 binonaria Ehr. (Mesocena) 283 bipartitus Lemm. (Cannopilus) 279 bisoctonaria Ehr. (Mesocena) 283 calyptra Hack. (Cannopilus) 269 — var. heptacanthus (Ehr.) Lemm. 270 — var. spinosa Lemm. 270, 280 * Names in italics are synonyms. Bold figures refer to pages [Russian, appearing in the left-hand margin Ba aa Hack. 224, 225, 271, 279, 280, 1 2 Chrysophyta 218 circulus Ehr. (Mesocena) Plate XXIX, 8 — var. apiculata Lemm. 278 — var. stellata (Hack) Lemm. 286 constricta (Schulz) Freng. (Naviculopsis) 257, 258 Corbisema Hanna 223, 225, 232, 233, 250, 252, 253 Cornua Schulz 220, 222 Cornuaceae Gem. 220 crenulata Ehr. (Mesocena) 285, 286 — var. diodon (Ehr.) Lemm. 284 — var. elliptica (Ehr.) Lemm. 284 cruz Ehr. (Dictyocha) 261 crux (Ehr.) Hack. (Distephanus) 260, 261, 263, 279 — f. aspera Schulz 261 — f. brevispina Schulz 261 — f. longispina Schulz 261 282, 285, var. apiculatus Lemm. 261 var. crux 261, Plates XVIII, 1—11; XIX, 1—6 var. mesophthalmus (Ehr.) Lemm. 263, 279 var. octacanthus Desikachary a. Mache- shwari 263 — var. schauinslandii (Lemm.) Schulz 263 — var. stauracanthus (Ehr.) Lemm. 263, 279 cyrtoides Hack. (Cannopilus) 274, 275, ’ — f. nonaria Schulz 274 deflandrei Freng. (Dictyocha) 226, 228, 239, 244, 246 — f. corbisemoidea Freng. 228 — f. heragona Freng. 239 — var. bicornuta Gleser Plate XII, 20—23 — var. completa Gleser 244, 246 — — f. completa 244, ra6m. XII, 14, 15 226, 246, — —f. producta Gleser 245, 246, taOm. XII, 17—19 — var. deflandrei 244, Plates XII, 13, 16; XXXII, 4 Dictyocha Ehr. 223, 224, 225, 230, 233, 235, 252, 253, 254, 260, 271, 274, 280 Dictyochaceae Lemm. 220, 223, 253 of this translation] where main descriptions are given. 358 Dictyochida 259 diodon Ehr. (Mesocena) 284 diommata Ehr. (Dictyocha) 269 Distephanus Stohr 224, 225, 259, Dhayecld; 2d, 202 260, elata Gleser (Dictyocha) 225, 237 — Var. elata 237,244, Plate X, J,.4 — var. media Gleser 238, 239 — — f. media 238, Plate X, 2, 3, 5 — — f. reducta 238, Plate X, 9 elliptica Ehr. (Mesocena) 282, 283, 285, Plates XXIX, 1—7; XXX, 1—5 elongata Gleser (Dictyocha) 225, 236, Plate XI, 1—7 epiodon Ehr. (Dictyocha) 247 fibula Ehr. (Dictyocha) 224, 226, 240, 241, 246, 247, 249, 250 forma Defl. 240, 244 f. aspera (Lemm.) Gem. 247 f. rhombica Schulz 245, 249 f. rotundata Schulz 241, 242, 246 f. speculum Freng. 261 var. aculeata Lemm. 250, Plate XV, 10 var. aspera Lemm. 247 var. brevispina Lemm. 247 var. fibula 245, 247 — f. eocaenica Krotov 249, 250, TAOS, DU s: On ROO, ga) — —f. fibula 247, Plates XIII, 6—9; XIV, 7—9 var. longispina Lemm. 247 var. messanensis (Hack.) Lemm. 251, es la a = | Plate XV, 8 — var. pentagona Schulz 250, Plate XV, 1—3 — var. rhombus (Hack.) Lemm. 252 aff. fibula — var. rhombus 201, Plate IX, 3 foliacea Freng. (Naviculopsis), 254, 257, 200. Plate” XVII oe frenguellii Defl. (Dictyocha) 226, 240, 241, 242, 260 — Lng carentis Gleser 237, 240, 241, 243, 2 — — f. carentis 240, Plates XI, 8, 10— 13? KX Te (Hack.) Lemm. — — f. incerta Gleser 241, 242, 243, Plate XI, 14—16 — var. frenguellii 240, 241, Plate XI, 9 furcata Jousé (Dictyocha) 225, 233, Plate XXXII, 6 furcula) Hanna (Lyramula) 220, 221, Plate II, 8, 5—7 — var. minor Defl. 224 geometrica Hanna (Corbisema) 230, 232, 252, 253, Plate IX, 7 — var. apiculata Jousé 229 haliomma Ehr. (Dictyocha) 269 hastata (Lemm.) Freng. (Corbisema) 227, 231 hastata Lemm. (Dictyocha) 232 hemisphaerica Ehr. (Dictyocha) 280, 284 hemisphaericus (Ehr.) Hack. (Cannopi- lus) 280, 281, XXVII, 1—4 — f. polyommata Schulz 280 heptacanthus Ehr. (Dictyocha) 269 heptagona Ehr. (Mesocena) 283 hexacantha (Schulz) Defl. (Corbisema) 239 hexacantha Schulz (Dictyocha) 226, 239, Plate we. Pe, hortonii Hanna (Vallacerta) 218, 219, 220, Platee ls hs XN KL, Plates XXVI, 1—5; iberica Defl. (Naviculopsis) 254 insolita Defl. (Nothyocha), Plate XXIV, 6 irregularis Hanna (Distephanus) 264 japonica Defl. (Dictyocha) 275, 276 japonicus (Defl.) Gleser (Distephanus) , 275 — f. japonicus 276, Plate XXV, 2, 9 — f. pseudofibula (Schulz) Gleser 276, Plate XXV, 1, 3—8, 10 lamellifera Gleser (Dictyocha) 225, 235, 237 — var. constricta Gleser 236, 15—17; XXXII, 2 — var. hastata Gleser 236, — var. lamellifera 235, Plates 14 XO aS Lyramula Hanna 220, 221 Plates X, Plate X, 10 xX, Mi, 13s Mesocena Ehr. 224, 282, 285 messanensis Hack. (Dictyocha) 251 minor Defl. (Lyramula) 221 minor (Schulz) Freng. (Naviculopsis) 256 muticata Gleser (Mesocena) 282, 285, Plate XXVIII, 4 navicula Ehr. (Dictyocha) 225, 233, 234, 235, 258; 201, 200,..Pinte 1X4, co — var. biapiculata Lemm. 253, 255, 256, 257 — — f. aspera Schulz 255 — — f. constricta Schulz 257 — — f. minor (Schulz) Gem. 256 — var. minor Schulz 256, 258 — var. trispinosa Schulz 256 navicula Defl. (Naviculopsis) 234, 254 Naviculopsis Freng. 223, 225, 234, 235, 237, 2593, 254, ‘250, 259 nonaria Ehr. (Mesocena) 284 oamaruensis Schulz (Mesocena) 282, 285 Plate XXVIII, 3 — var. apiculata Schulz (Mesocena) 283 obliqua Gleser (Dictyocha) 226, 246, Plate XIII, 1—5 octogona Ehr. (Mesocena) 283 octogonius Hack. (Distephanus) 272 octonaria Ehr. (Dictyocha) 272, 273, 274 octonarius (Ehr.) Defl. (Distephanus) 260, QT DIZ, Zid, Bits: al dpacou — var. cyrtoides (Hack.) Gleser 274, 275, Plate XXV, 11 — var. octonarius 272 — var. polyactis (Jérg). Gleser 273, 274, Plate’ “Ay if, o ornamentum Ehr. (Dictyocha) 264, 268 ornamentum Hack. (Distephanus) 264 359 Paradictyocha Freng. 224, 274, 276, 278, 279, pentagona Hack. (Mesocena) 284 polyactis Ehr. ren eel ge Ohi; 2s — f. mesocenoidea Def). polyactis (Ehr.) Defl. biiasteptidadiny i 278 — f. mesocenoidea Defl. 278 polyactis (Ehr.) Freng. (Paradictyocha) 276 — f. completa Freng. 277 — f. mesocenoidea Freng. 277, 278, Plate XXVIII, 7 — f. polyactis 274, 277, Plate XXIV, 7—I11 — f. reducida Freng. 279 polymorpha Lemm. (Mesocena) 285 var. binonaria (Ehr.) Lemm. 282 var. bioctonaria (Ehr.) Lemm. 282 var. heragona (Hack.) Lemm. 284 — f. octonaria Schulz 284 — f. septenaria Schulz 284 var. pentagona (Hick.) Lemm. 284 var. quadrangula (Ehr.) Lemm. 284 var. triangula (Ehr.) Lemm. 283, 284 ponticulus Ehr. (Dictyocha) 234 poretzkajae ipgtine (Cornua) 222, Plate III, pulchra Schiller reece 272 Teele te iets thet quadralta (Hanna) Defl. (Corbisema) 253 quadrangula Ehr. (Mesocena) 284 robusta Defl. (Naviculopsis) 254, Plates XVI, 1; XXXII, 3—6 rotundata Jousé (Dictyocha) 220.4 2305 242, 243, 260 — var. rotundata 243, Plate XI, 17—20 — var. secta Gleser 243, Plate XII, 1—6, UA AR rotundus Stohr (Distephanus) 264 ruestii Defl. (Corbisema) 253 schauinslandii cha) 247 schulzii Defl. (Phyllodictyocha) Plate IX, 6 septenaria Ehr. (Dictyocha) 268 siderea Schulz (Dictyocha) 219 — var. quadrata Schulz 219 Silicoflagellatae Borgert 218 Silicoflagellatophyceae 218 (Lemm.) Freng. (Dictyo- simplex Hanna (Lyramula) 221, Plate II, we ged simplex Jousé (Vallacerta) 218, 249, Plate I, 2 Siphonotestales Lemm. 218, 220 speculum Ehr. (Dictyocha) 259, 264, 267, 268, 270, 274 — f, cannopiloides Pr.—Lavr. 269, 274 — f. octonarius Jorg. 272 — f. polyactis (Ehr.) Jérg. 273 — f. pseudofibula Freng. 247 — f. septenarius (Ehr.) Jorg. 268 — formae 1—6 Tynan 270 — var. septenaria Ehr.after Tynan 270 speculum (Ehr.) Hack. (Distephanus) 260, 263, 266, 268, 270, 271, 273, 274, 275, 276, 281, 282, Plates xis: y ae Ge XX, ca — f. eis Schulz 264 — f. pseudocrux Schulz 275, 276 — 7 pseudofibula Schulz 275, 276 var. aculeatus (Ehr.) Lemm. 264 — var. brevispinus Lemm. 264, 266 — var. cannopiloides 269, Plates XXII, 1—5; XXIII, 1—6; XXIV, 1—5 var. heratyra (Ehr.) Lemm. 264 es octonarius (Ehr.) Jorg. 272, 273, 27 — f. coronata Schulz 272 — f. octogenia (Haick.) Lemm. 272 — f. polyactis Jérg. 273, 274 var. pentagonus Lemm. Plate XXI, 1—5 — f. armata Lemm. 267 var. polyactis Lemm. 273, 277 — f. decagona Zanon 277 . dodecagona Zanon 277 . endecagona Zanon 277 regularis Lemm. DW liad — f. coronata Schulz 266 var. septenarius (Ehr.) Joérg. 268, Plate XXI, — var. speculum Phy 265, 271, Plates XIX, 7—9; XX, sphaericus cha Plae XXVII spinosa Defl. fcoraetias 238, 253 spinosa (Defl.) Gleser (Dictyocha) 225, 238, 240, Plate X, 6—8 stauracanthus Ehr. (Dictyocha) 263 stauracanthus (Ehr.) ar (Distephanus) 260, 263, Plate XIX, staurodon Ehr. (Dietyccha) 245 staurodon Ehr. (Dictyocha) 244 stellata Hack are 282, 286, Plate XXVIII, 271, 1 | [fee 267, eae ae 9 tal | hr 266, 267, (Cannopitus 280, 281, transitoria Defl. (Dictyocha) 225, 242, 246, 260, Plate XII, 7—10 triacantha Hanna (Corbisema), 226, 253 — f. dictyoquidea Freng. 249 — var. fleruosa Stradner 228 triacantha Ehr. (Dictyocha) 225, 226, 220, 200s BON; 250. Daag ele var. apiculata Lemm. 228, 229, 232 — f. apiculata 228, 230, Plate VI, 5 — f. aspera Schulz 228 — f. late-radiata 229, Plate VI, JZ — f. minor Schulz 229, Plates VI, 2—4,; XXXI, 4—6 — var. archangelskiana Schulz 232 — var. eocaenica Krotov 236 — var. flexuosa (Stradner) Gleser 228, TAOH. “V,, 5,16, 05,00 — var. hastata Lemm. 231, 232, 236, Plates VI, 6—8; VII, 1—8; XXXI, 8—9 var. hastata Lemm. 284 var. inermis Lemm. 230, 232, 235 — f. inermis 230, 234, Plates VIII, 1, 2; ». ©, OG |) et | — — f. minor Gleser 230, VIII, 38—5; XXXI, 7 — var. triacantha 225, 226, 232 — — f. minor Schulz 227, Plate V, 7, 9 — — f. triacantha 226, 229, Plates IV, 1—6; V, 1—4; XXXI, 2, 3 triangula Ehr. (Mesocena) 283 | Plates 360 triangularis Stohr (Lithocircus) 284 tumidula Gleser (Vallacerta) 218, 220, trifurcata Schulz (Cornua) 222, 223, taOa. I, 3—6 Plate III, 3—5 trigona (Zittel) Defl. (Corbisema) 227 Vallacerta Hanna 218 trigona Zittel (Dictyocha) 226 Vallacertaceae Defl. 218 triommata Ebr. (Dictyocha) 226, 269 Vallacertales Gleser 218 triommata (Ehr.) Lemm. (Cannopilus) 270 Vallacertidae Defl. 218 tripartita Ehr. (Ebria) 231 variabilis Hanna (Distephanus) 250, 267, trispinosa (Schulz) Gleser (Naviculopsis) 270, 274 254, 258, Plate XVII, 7 361 EXPLANATORY LIST OF ABBREVIATED NAMES OF USSR INSTITUTIONS, PERIODICALS, ETC. Abbreviation BIN AN SSSR Bot. mater. Otd. spor. rast. BIN AN SSSR Byull. Komiss. po izuch. chetvert. perioda Ezhegodn. geol. i mineral. Rossii Inform. sb. VSEGEI LGU Mater. po geol. i polezn. iskop. reals: MGU Novosti sist. nizsh. rast. SNIIGGIMS SO AN SSSR TINRO Full name (transliterated) Botanicheskii institut Akademii Nauk SSSR Botanicheskie materialy Otdela sporovykh rastenii botanicheskogo instituta AN SSSR Byulleten' Komissii po Izucheniyu chetvertich- nogo perioda Ezhegodnik po geologii i mineralogii Rossii Informatsionnyi sbor- nik Vsesoyuznogo geologicheskogo instituta Leningradskii gosudarstvennyi universitet Materialy po geologii i poleznym isko- paemym Urala Moskovskii gosudarst- vennyi universitet Novosti sistematiki nizshikh rastenii Sibirskii nauchno- issledovatel'skii institut geologii, geo- fiziki i mineral'nogo syr'ya Sibirskoe otdelenie Akademii Nauk SSSR Tikhookeanskii nauchno- issledovatel'skii institut rybnogo khozyaistva i okeanografii 362 Translation Botanical Institute of the Academy of Sciences of the USSR Botanical Materials of the Department of Cryptogenic Plants of the Botanical Institute of the Academy of Sciences of the USSR Bulletin of the Commission for Studying the Quaternary Yearbook on Geology and Mineralogy of Russia Informational Collection of the All-Union Geological Scientific Research Institute Leningrad State University Materials on the Geology and Mineral Resources of the Urals Moscow State University Advances in the Systematics of Lower Plants Siberian Scientific Research Institute for Geology, Geophysics and Mineral Ores Siberian Branch of the Academy of Sciences of the USSR Pacific Scientific Research Institute of Marine Fisheries and Oceanography Abbreviation Trudy VNIGRI Mech. zap. LGU, ser. biol. nauk. Vestn. LGU VSEGEI Zap. Novoross. obshch. estestvoispyt. Full name (transliterated) Trudy Vsesoyuznogo neftyanogo nauchno- issledovatel'skogo geologo-razvedochnogo instituta Uchenye zapiski Leningradskogo gosu- darstvennogo univer- siteta (seriya biolo- gicheskikh nauk) Vestnik Leningradskogo gosudarstvennogo universiteta Vsesoyuznyi nauchno- issledovatel'skii geologicheskii institut Zapiski Novorossiiskogo obshchestva estestvo- ispytatelei 363 Translation Transactions of the All- Union Petroleum Scientific Research Institute for Geological Prospecting Scientific Reports of the Leningrad State University (Series of Biological Sciences) Bulletin of the Leningrad State University All-Union Geological Scientific Research Institute Reports of the Novorossiisk Society of Naturalists é rape 7 Ve Ae Retin ne | 7 ‘ise “3 iva ea 7 Po eo ET st oy fo ai foal oe Rai ; ro 7 pny i 7 f ¢ he, aM .* . s! 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