Hungarian Geological Institute M. Kazmer ABSTRACTS

Teljes szövegt

(1)IN TE R N A TIO N A L A S S O C IA T IO N OF S ED IM EN TO LO G IS TS H U N G A R IA N G E O LO G IC A L S O C IE TY. ABSTRACTS Edited by. M. Kazmer. Published by. Hungarian Geological Institute.

(2) INTERNATIONAL ASSOCIATION OF SEDIMENTOLOGISTS. 10th IAS REGIONAL MEETING ON SEDIMENTOLOGY. organized by the. Committee on Sedimentology of the Hungarian Academy of Sciences in cooperation with the Geological Society of Hungary.

(3) SPONSORS. The Organizing Committee of the 10th IAS Regional Meeting on Sedimentology gratefully acknowledges the financial support of the following organizations:. Ministry of Industry Ministry of Environmental Protection Management. and Water. Ministry of Food and Agriculture Hungarian Academy of Sciences Central Office of Geology National Oil and Gas Trust Hungarian Aluminium Trust. Designing and General Contracting Company for the Oil Industry Dorog Coal Mines FTV Consulting Engineering Gephysical Prospecting Company Hungarian Geological Institute Hungarian Hydrocarbon Institute Hydrocarbon Exploration Company Mátraalja Coal Mines Oil and Gas Production Company of the Hungarian Great Plain Oroszlány Coal Mines Petroleum Exploration Company Veszprém Coal Mines.

(4) ABSTRACTS.

(5)

(6) 10th IAS REGIONAL MEETING ON SEDIMENTOLOGY - BUDAPEST, 1989. CONTENTS (P = POSTER) P. ARACIL, E. Use of Well Logs as a Stratigraphic Tool in Carbonate Series: an example in Southern Iberian Ranges (Spain) . 1. P. ARRIBAS, M.A. - FERNANDEZ, J.C.G. - MELENDEZ, N. (Madrid): Early diagenetic processes in lacustrine and in related flood plain sediments from the Lower Cretaceous /Central Spain/ ...................................................... 3. BADILLO-LARRIETA, O.M. - GARCIA-GARMILLA, F. (Bilbao): Petrology of the Terrigenous Middle-Upper Albian Series /BasqueCoast, Northern Spain/ ................................... 5. BADINSZKY P. - MÉSZÁROS M. - SZABÓ Cs. (Budapest): Results of complex sedimentological prospecting of secondary raw materials in Hungary ...................................... 7. P. BAHLBURG, H. (Berlin): The Ordovician sediments in the Northern Puna of Argentina: Correlation of sedimentologic, tectonic and sea level change events ............................ 8 BAKHTUROV, S.: Cambrian black shale formations of the Siberian platform .................................................. P. 10. BALOG A. - HAAS J. (Budapest): Diagenetical history of Dachstein Limestone in the vicinity ofVác ......................... 12 BASTIDA, 0.(Valencia) - MACIAS, I.(Terrassa) - ESTRADA, R. (Barcelona) - RAMPONE, G.(Barcelona): Clay mineralogy of the lutites of Peraltilla Formation /Oligocene, NE Spain/13 BEAUDOIN, B. - EL MAHERSSI, Ch. (Fontainebleau): Major erosional discontinuities in theNumidian flysch of Tunisia ...... 14 BEAUDOIN, B. - MAILLARI, J. - MERCIER, D. (Fontainebleau): Bedding and pseudo bedding in alternating limestones and marls': origin and age in Middle Domerian, S. France ... 16 BEAUDOIN, B. - PARIZE, 0. (Fontainebleau): Differential mechanical behaviour during diagenesis and compaction in an alternating marl-limestone formation ............... 18. P. BELAK, M. - PAVELIC, D. - SLAT, M.S. (Zagreb): An Occurence of Badenian of Rhyolitic Volcanoclastic Rocks in the Middle Part of Dilj Mountain /Eastern Croatia/ ............... 20. P. BELLOTTI, P. (Roma) - CHIOCCHINI, U. (Viterbo) - CIPRIANI, N. (Firenze): - MILLI, S. (Roma): Sedimentological characters of the Pleistocene gravelly-sandy beaches in the surroundings of Rome, Italy ........................... 22. iii.

(7) P. P. BERNÁTH Z. - TARNÓCZI F. (Budapest): Sediment-geological experience of mineral raw material prospecting for the building material industry ............................ ' 24. BILLI, P. - MAGI, M. - SAGRI M. (Florence): Lacustrine fandelta deposits of the Plio-Pleistocene Valdarno Basin, Italy ................................................... 25. BLAGOVIDOV, V.: Facies environments of epicaledonian inter continental carbonate basins (USSR) .................. 27. BDULVAIN, F. (Orsay): Cementation of cavities in Middle Frasnian micritic mounds (Belgium, France) ........... 29. BÜHM, F. (Erlangen): Liassic Palaeogeography of the North eastern Calcareous Alps ................................ 31. BRACHERT, T.C. - DULLO, W.Ch. (Erlangen): Modern and Triassic carbonate slope "stromatolites" ....................... 32. BRÜCKNER, S. - LANGBEIN, R. (Greifswald): Distribution of Mn ............ in carbonatic rocks of Eastern Thuringia. 33. CAPUANO, N. - TONELLI, G. - VENERI, F. (Urbino): Sedimentological and Paleoenvironmental Significance of armored mud balls in the Pliocene deposits of the Adriatic Foredeep (Italy): ............................ 35. P. CARANNANTE, G.(Napoli) - CHERCHI, A.(Cagliari) - D'ARGENIO, B. (Napoli) -SCHROEDER, R .(Frankfurt-Main) - SIMONE, U (Napoli) : Restricted to open shelf carbonate sedimentation in northwestern Sardinia /Italy/ ..................... 37. P. CARANNANTE, G. - D'ARGENIO, B. - FERRERI, V.(Napoli) - i MINDSZENTY A. (Budapest) - SIMONE, L.'(Napoli): Ephemeral and long lasting emersion episodes and related paleokarst and bauxites in the Cretaceous carbonates of Southern Apennines /italy/: 39 CAVAZZA, W. (Bologna): Miocene detrital modes and geodynamics of the Calabria - Peloritani Arc /Southern Italy/ .... 41. CHEN, X. (Beijing): Dolomitization and Diagenetic History of Massive Dolomites in the late Precambrian Carbonate Sequences, Xuhuai Region /East China/ ................ 42. CHIGCCHINI, U. (Viterbo) - CIPRIANI, N. (Florence): Provenance and evolution of the Miocene turbidite sedimentation in the Central Apennines .................................. 44. CHOCHOV, S.D. - SHANOV, S.B.: Findings of Holocene sapropel breccia in the bottom sediments of the Western half of the Black Sea ............................................ 46. CICHOVSKY, L. - BYLOVÁ, I. (Prague): Argillogenesis in the sedimentary basins of region Bohemian massif /Czecho slovakia/ ............................................... 48. IV.

(8) CICHOVSKY, L. - DAVIDOVÁ, P. (Prague): The kvantitative determination of structural arrangement of sedimentary rocks various types and facies .......................... 50. CLEMMENSEN, L.B.: Interdraa and draa plinth deposits of the Early Permian Sand Sea/Yellow Sands/, NE England ...... 52 P. COCCO, E. - DE PIPPO, I. - VALENTE, A. (Napoli): Evolution of the Pollica Sandstone Turbidite Basin /Cilento Flysch, Southern Apennines/ ...................................... 54. COSOVIC, V. - TOMIC, V. (Zagreb): A characteristic sequence of Doggerian microfacies in Gorski Kotar /Western Croatia, Yugoslavia/ .............................................. 56 COWAN, G. (London): Maturation modelling and diagenetic histories of Namurian Sandstones, East Midlands Basin and Southern North Sea Basin ......................................... 58 CSÁSZÁR G. (Budapest): Transgressive urgonian facies with "black pebbles" from the Villány M t s ............................. 59 CSATÓ I.: Pannonian sedimentological facies relations of the hydrocarbon accumulations within the central part of the Pannonian basin .......................................... 60 P. CSERNY T. - CORRADA, R. : Sedimentary Maps of the Lake Balaton. 63. CSIRIK Gy. - SOLTI G.: The depositional position of the alginite in a basaltic tuff maar crater at Village Pula /Transdanubian Mountains, West-Central Hungary/ ............. 64 P. D'ARGENIO, B. - FERRERI, V. (Napoli): New data on Southern Italy Travertines: textures and depositional environments ... 66. P. D'ARGENIO, B. (Napoli) - MINDSZENTY A. (Budapest): "MidCretaceous" regional unconformities and related bauxites/ paleokarst of the Mediterranean. Results of distant and proximal tectonic events? ............................... 68. P. DE MIGUEL, 3.L. - MARTINEZ, F.3. - SANCHEZ, 3 . A. - SAN ROMAN, 3. (Zaragoza): Mobilization and transport of solutes by groundwater, an example the Iberian chain drainage into the Tertiary Ebro basin /Spain/ ........................ 70. P. DEVILLE, Q. (Geneva): New observations on "Keystone vugs": their formation and preservation in recent beaches, and consequences for interpreting ancient sedimentary deposits .................................................. 72. DOLENEC, T. - HERLEC, U. - PEZDIC, 3. - MISIC, M. (Ljubljana): The Oxygen and Carbon isotopic composition of modern rhodolithes from the Murter Sea /Middle Adriatic/ ..... 74. D0L0T0V, Y.: On the pecularities of lamination in the near shore marine sedimentary strata ......................... 76. DONGAROV, E.G. - NAMESTNIKOV, Y.G.: Geodynamic approach to Neogene palaeogeography ofCarpathian region ............ 78 EL-FISHAWI, N. - BADR, A.: Estimation of drift rates on accreted and eroded beaches by fluorescent sand, Nile Delta coast /Egypt/ .................................................. BO. v.

(9) ENOS, P. - JIAYONG, W. - YANG3I, Y. : Platfrom margin collapse and slope retreat, Mid-Triassic, Guizhou, China ....... 82. EVANS, M.(Liverpool) - MANGE-RA3ETZKY, M.(Oxford): Depositional Systems and Heavy Mineral Suites in the Barreme Foreland Basin, Haute-Provence, France ......................... 83 P. FALK, F. - HAHNE, K.: Heavy minerals and trace elements in the Paleozoic of Thuringia /GDR/ ............................ 83. P. FEISTNER, K.(Cambridge): A quick and easy method for obtaining carbon /inorganic and organic/ and sulphur contents of mudrocks? ............................................... 87. P. FE3ES I. - CSERNOSSI G.:. In situ testing in sedimentology. .... 89. FORNOS, 3.J. - FORTEZA, V. - JAOME, C. - MARTINEZ-TABERNER, A.: Fornells Bay /Northern Menorca, Spain/: An Example of Restricted Sedimentation in a Temperate Carbonate Shelf. 90. FOCHS, A. (Goldberg): Relationship between facies development, conodont stratigraphy and colour alteration indices of conodonts in the Elbingerode Reef Complex, Harz Mountains /Devonian - Lower Carboniferous/ ....................... 92 P. GARCIA-GARMILLA, F. - AROSTEGUI, 0. - HERRERO, 3.M. (Bilbao): The Lower Wealden Sediments of Bilbao suggest a Lacustrine/ Evaporitic Environment /Lower Cretaceous, Basque-Cantabrian Region, Northern Spain/ ................................. 94. P. GARCIA-GARMILLA, F. - BADILLO-LARRIETA, 3.M. (Bilbao): Lower Cretaceous Fluvio-Lacustrine Systems in Burgos /BasqueCantabrian Region, Northern Spain/ ...................... GASIEWICZ, A. : Event sedimentation in the Zechstein Platy Dolomite tidal flat complex of the Leba Elevation /N Poland/ .................................................... GEORGIEV, V.M. : Recent carbonate cementation of beach and marine sediments in the Bulgarian Black Sea shelf .... 96. 98 100. GLENN, C.R. (Zürich): Sedimentology and geochemistry of sedimentary facies in a Cretaceous Tethyan phosphorite giant: comparisons with modern environments ............. 102. HAAS 3. (Budapest): Stages of Upper Triassic carbonate platform development on the Tethys shelf ................. 104. HÁMOR T. (Budapest): The occurences and morphology of sedimentary pyrites ..................................... 106. HORVÁTH A. (Budapest): Diagenesis and fluorescence patterns in the Nagyharsány Limestone Formation /Barremian-Aptian/ from drill-holes /S-Hungary/ ......................... P P. vi. 108. HORVÁTH A. (Budapest): Fluorescence in deep-buried Mesozoic carbonates, S-Hungary ' ............... ... ................ 109. HORVÁTH A. - MOLNÁR F. (Budapest): Near-surface and burial diagenesis of Mesozoic carbonates in some hydrocarbonexploring drillings from S-Hungary as revealed by fluorescence microscopy and fluid inclusion studies ... 110.

(10) JACOBS, P. - SEVENS, E. (Gent): Sedimentology of the Eo-01igocene layers in Northwest Belgium ......................... 112 JANSSEN, Ch. - PAECH, H-J.: Diagenesis and recrystallization of the Devonian reef limestone of the Elbingerode Complex, Harz Mountains /GDR/ ................................... 114 JIANG, N.: Sedimentary facies and mineral deposits in North Xinjiang, China ....................................... 117. JUHÁSZ E. - BÁRD0SSY Gy. (Budapest): Comparative sedimentological study of karst bauxite in the Halimba area, Hungary 118 JUHÁSZ Gy.- SZENTGYORGYI K.: Sedimentological characterictics of the Neogene sequences in SW Transdanubium, Hungary. 12D. JUOZAPAVICIUS, G.: Evolution of disintegrated material during formation of Quarternary continental deposits in the western part of the USSR .............................. 121. KARNYUSHINA, E. - CHOCHIYA, G. (Moscow): Processes and conditions of formation of sediments on the Pacific margin of Kamchatka .......................................... 123 KHABAROV, E. (Novosibirsk): buildups of Siberia. Precambrian organogenic carbonate .................................. 125. KHANDAKER, N.I.(Ames) - SUTTON, R.G.(Rochester): Western boundary undercurrent and deep water facies off Nova Scotian continental margin, Canada .......................... 127 KHEDR, E. - FELESTEEN, A.W. - ABUL-MAJD, K. - IBRAHEEM, K.: Recent and ancient analogues of coastal sabkhas from the Red Sea marginal area ................................ 129 KOPRIVICA, D.: Loessoide sandy silts in the Senta - Kikinda area /Yugoslavia/ ..................................... 131. KOZUHAROV, E. - GEORGIEV, V.: Early stage in the formation of ferro-manganese nodules in the outer Bulgarian Black Sea shelf .............................................. 133. KOVÁRINÉ GULYÁS E.: Engineering geological mapping of sedimentary rocks in settlements having cellars' ................ 135 KRAINER, K. (Innsbruck): Evolution of the "Badstubbreccia" in the Carboniferous of Notsch /Eastern Alps, Austria/. 137. KUZNETSOV, V.G. (Moscow): The influence of tectonics and climate on the structure of carbonate formations .......... 139 KUZNETSOV, V.G. - POSTNIKOVA, O.V. - ILYUKHIN, L.N. (Moscow): Organic build-ups of the Lower Cambrian of the South of the Siberian platform ................................. 141. LIANG,C. (Beijing): Sedimentary facies character of Phosphorus Bearing system of the Doushantuo Formation and distribution regularities of Phosphorite Deposits in Yichang, China 142 LESZCZYNSKI, S. (Krakow): Depositional models of the Polish Carpathian Flysch coarse elastics /Cretaceous-Miocene/. 144. LUTZNER, H.: Tempestites in Lower Palaeozoic shelf deposits of 146 Thuringia /GDR/ .......................................

(11) MA, Y.:. The Sphere of Storm Action, the Distributional Area of Storm Deposits and the possibility to take Tempestites as isochronic surface in geological time ........... 148. MARTIN-CHIVELET, J. - GIMENEZ, R. (Madrid): Sedimentary and pedological features on microtidal sequences in limestones: an example in Upper Cretaceous of Prebetic Ranges /SE ................................................ 149 Spain/ MCLEAN, J.R. /Rijswijk): Recognition of Estuarine Deposits in the Geological Record ................................ 151 MASTALERZ, K.: Lower Permian Lacustrine succession, Anthracosia Shales, /North-Sudetic Basin, SWPoland .............. 152 MASTALERZ, M. ¡(Wroclaw): Depositional environment of the coal seams of the Walbrzych Formation, Intrasudetic Basin, SW Poland ............................................. 154 MASTALERZ, K. (Wroclaw): Foreset beds on a Neopleistocene fluvioglacial Gilbert-type body,Eastern Poland ______. 155. MASTALERZ, K. - WOJEWODA, J. (Wroclaw): Rotliegendes sedimentary basins in the Sudetes /SW Poland/: structural, sedimentary and climatic evolution ............................... 156 MERZLYAKOV, G.: Platform. Upper Precambrian sulphates of the Siberian ............................................... MINDSZENTY A. (Budapest): New trends in karst bauxite geology ................................................ 158 160. MINDSZENTY A. (Budapest) - SZINTAI M. - SZANTNER F. - NAGY I. GELLAI M. - BAROSS G. (Balatonalmádi): Sedimentology and depositional environment of the Csabpuszta bauxite /Paleocene-Eocene/ in the Bakony Mts. /Hungary/ ... 162 MOLINA, J.M. - RUIZ-ORTIZ, P.A. - VERA, Ü.A. (Granada): Jurassic karstic bauxites in the Subbetic of Southern Spain .................................................. 164. MOLNÁR B. - FÉNYES J. (Szeged): Moderne lacustrine carbonate depositional environments in the Danube-Tisza Inter fluve ................................................. 166 MUNOZ, A. - PEREZ, A. - VILLENA, J. (Zaragoza): The open lacustrine facies of Villarroya Pliocene basin /La Rioja province, N of Spain/ .......................... 168. IVAN, N. - CHAVDAR, N. (Sofia): Genetic model of bedded cherts in Emine flysch /Bulgaria/ .......................... 170 NÁDOR A. (Budapest): Triassic-Jurassic boundary formations of South Gemericum /Inner West Carpathians/ .......... 172. NIEDERMEYER, R.O. (Greifswald): Modern organic-carbon rich mud deposition of the Western Baltic Sea - a conceptual model ................ 174 NOE-NYGAARD, N. - SURLYK, F. (Copenhagen): Washover fan, brackish bay sedimentation, and bivalve mass mortality caused by toxic dinoflagellate blooms in the Berriasian-Valanginian of Bornholm, Denmark ................................. 176.

(12) NOVIKOV, V.P. - SUPRYCHEV, V.V.: Sedimentation, volcanism and ore's formation during the Permian in the Northern Pamirs .................................................... 177. OLLIER, G. - COCHONAT, JJ.F. (Plouzané) - LENAT, B. (ClermontFerrand) - SAVOYE, P. (Plouzané) - BACHELERY, P. (La Réunion) - BOIVIN, P. (Clermont-Ferrand) - CORNAGLIA, B. (paris) - DENIEL, C. (Plouzané) - LABAZOY, P. (Plouzané) LIPMAN, P. (Denver) - VINCENT, P. (Clermont-Ferrand) VOISSET, M. (Plouzané): Sedimentary processes on the submarine flanks of a volcano /Piton de La Fournaise, Reunion Island/. Preliminary results of a sidescan sonar cruise ................................................... 179 PÁLINKÁS, A.L. - PAVUSEK, I. (Zagreb): Recognition of watertable position by means of Fe, Mn-incrustations. A case study in recent and paleofluvial environment .................. 181 PAP S. (Szolnok): Anisian /Middle Triassic/ strata in SE part of area between Danube and Tisza and their importance as hydrocarbon reservoirs ................................. 183 PARAEV, V.: Red-coloured complex of Cenozoic deposits of the Pamir-Alai /USSR/ ...................... .................. 184. PEDERSEN, G.K. (Copenhagen): Delta plain sequences in the Cretaceous of the West Greenland Basin ................... 186 P. PFEIFFER, 3. (Zürich): Sedimentology of a condensed sequence /Altmann Mb./ and sequence stratigraphy in the Lower Cretaceous /Drusberg Fm., Helvetic Realm, Switzerland/. 188. POGÁCSÁS Gy. (Budapest) - KÁDÁR-3UHÁSZ Gy. (Százhalombatta) LAKATOS L. (Budapest) - RÉVÉSZ I. (Százhalombatta) U3SZÁSZI K. (Budapest) - VÁRK0NYI L. (Budapest) - VÁRNAI P. (Budapest) - VAKARCS G. (Budapest): Neogene seismic and electro facies of the Pannonian Basin ................. 190 PREAT, A. - DE PUTTER, Th. (Bruxelles): Subaerial crusts, ooids and breccia horizons in Upper Visean of Namur Basin /Belgium/: Sedimentology and diagenesis .............. 192 RIEZEBOS, P .A. - KATE, W.G.H.Z. - DE BRUIN, M . : Raseneisenerz concretions in Luxembourg, eluvial products of iron crusts developed in the Minette Formation ............ 194. RODRIGUEZ-PEREA, A. (Palma de Mallorca): Miocene mixed shelf deposits of Mallorca Island ............................. 196. RUSKOVA, N.: Early Cretaceous sedimentary evolution in NorthWestern Bulgaria ......................................... 199. RUZICKOVA, E.: Lithology and genesis of Late Cenozoic sediments in the NE part of the Krusne Hory Mts. /Northern Bohemia/ ................................................. 201 SAVIC, D. (Zagreb): The Peridinaridic Carbonate Platform evolution and old basements ............................. 203. SAVOYE, B. - COCHONAT, P. - OLLIER, G. - AUFFRET, G.A. BOURILLET, 3.F. (Plouzane): The Submarine Var Canyon /French Riviera/: Detailed Study of the Activity of a Modern Canyon ............................................ 205. IX.

(13) P. SCHIAVON, N. (Cambridge): Gypsum crusts formation and "stratigraphy" on weathered building limestones. .... 207. SCHIRRMEISTER, G. (Greifswald): Facies differentation in carbonate rocks during the Upper Devonian in the region of Eastern Thuringia /GDR/ ........................ 209 P. SEDLETSKI, V. - BAIKOV, A. - SEMENOV, G. (Rostov): Tectonics and Halogenesis ..................................... 211 SHIMKEVICHIUS, P. - ROTKYTE, L.: Kaolinite and depositional environments of Jurassic deposits in Baltic region 213 SLIWINSKI, W. (Wroclaw): Shallowing-upward carbonate sequences in a nontidal, pre-evaporite,basin /Zechstein Limestone, SW Poland/ ........................................... 215 P. SOLTI G. - VETŐ I. (Budapest): Lithology and geochemistry of the lacustrine sediments filling the Pula basalt tuff crater /Upper Pliocene, Hungary/ - Implications for ................................... 217 paleoenvironment SOUSSI, M. - M'RABET, A. - RABHI, M. (Tunis): The Jurassic series of Central Tunisia: an example of shallow to deep marine carbonate shelf ........................... 220 S0VET0V, J. - BUTAKOV, E. : Upper Riphean flysch of the Yenisei Mount /South-Western margin of the Siberian Platform/ ............................................. 222. STATTEGGER, K. (Graz): Heavy mineral events and tectonostratigraphy The case study of the Neogene Styrian basin /Austria/ 224 STRASSER, A. ^ DAVAUD, E. - KINDLER, P. - MARTINI, R. (Geneva):: Transgressive-regressive depositional sequences in Upper Pleistocene /Tyrrhenian/ coastal sediments of Sardinia,Italy .......................... 226. SULTANOV, A.T. (Sofia): Sarmatian algal stromatolites from NE Bulgaria ........................................... 228. SURLYK, F. - NOE-NYGAARD, N. (Copenhagen): Shelf,and ridges, banks and sandwave fields from the Volgian-Valanginian Raukelv Formation ofJameson Land, East Greenland 229 P. SZENTGYÖRGYI K.: Sedimentological and Faciological Characteristics of the Senonian Pelagic Formation of Hungarian Plain ................................... 230. SZTANÚ 0. (Budapest): Middle Cretaceous submarine channelfilled conglomerate in the Gerecse Mountains, Hungary 231 TARI G. - LEÉL-ŐSSY Sz. - SZTANÓ 0. (Budapest): Sand waves in the Early Miocene Pétervására Sandstone, Northern Hungary .............................................. P. 233. TÓTH K. (Balatonalmádi): Sedimentology of the Middle Eocene Szőc Limestone Formation of an investigated area in the Northern Bakony range /Transdanubia, Hungary/ .... 235 TÖRÖK Á. (Budapest): Sedimentary Analysis of an Upper Jurassic Calcareous oolite, Villány Mts., SouthHungary ............................................... x. 237.

(14) P. TSVETKOVÄ-GOLEVA, V.: The role of Bulgarian Black Sea coast's landslides in accumulation of heavy minerals ......... 239 TUCKER, M. (Durham) - CALVET, F. (Barcelona) - MARSHALL, 3. (Liverpool): Triassic /Upper Muschelkalk/ reef-mud mounds, Catalan Basin, Spain: early marine diagenesis and dolomitization ...................................... 241. UCHMAN, A.: Development of Jurassic carbonate sedimentation in the Choc unit, the Tatra Mts., Poland ............. 243 VECSEI, A. - EBERLI, G.P. (Zürich): Depositional geometry of prograding carbonate sands along the upper slope of Maiella carbonate platform /Central Italy/:. 244. VELEV, V.: Morphology of the continental slope and structure of Holocene sediments in the Western part of the Black Sea ...................................................... 246 P. VICZIÄN I. (Budapest): Clay mineralogy of genetic types of Hungarian sedimentary rocks ............................. 248. VÖRÖS A. (Budapest): Fault-scarp controlled carbonate sedimentation in a Tethyan Jurassic seamount area/Bakony, Hungary/ 250 WAGREICH, M. (Vienna): Basal conglomerates of the Gosau Group /Senonian/ of Austria: alluvial sedimentation in small rapidly subaiding, fault-bounded basins .............. 252 WINKLER, W. - BERNOULLI, D. (Zürich): Sedimentary evolution and provenance of South Alpine flysches: Palaeotectonic implications ........................................... 253 WOJCIK, A.: Sedimentology of Devonian and Carboniferous deposits in the Opawskie Mountains, Poland .......... 254. WOJCIK, A.: Geological characteristics of Silurian deposits in the Myszkow-Zawiercie area /Silesia-Cracow region, Poland/ ................................................. 255. WOJCIK, A.: Analysis of geological information from sedimentary sequences ..................................... 256 W0JEW0DA, J. (Wroclaw): Formation and structure o f ’a lacustrine alongshore bar: Recent example from Turawa Lake, SW Poland ................................'•....... 257. P. YU, J. (Zürich) - CHEN, K. (Xining): The sedimentary environment of Qarhan Playa in the Qaidam Basin, North west China ............................................. 258. P. YUSTA, I. - AROSTEGUI, J. - GARCIA-GARMILLA, F. - HERRERO, J. M. - VELASCO, F. (Bilbao): Sedimentation and Diagenesis in the Villaro Wealden /Lower Cretaceous, BasqueCantabrian Region, Northern Spain/ .................... 259 ZANIN, Y. - ZVEREV, K. - SOLOTCHINA, E.: Clay minerals as indicators of phosphorite formation of the inland epicontinental seas .................................... 261. ............ 262. ZHARKOV, M.A.:. Models of evaporite sedimentation. ZWENGER, W.H. (Fürstenwalde): Sedimentary environment of Lower Muschelkalk /Triassic/ at the basin-central position of Ruedersdorf /GDR/ ..................................... 263 XI.

(15) LATE ARRIVALS. CHARLES, C.(Toulon) - COCHONAT, P.(Brest) - GREGER, В. (Hannover) - HOFFERT, M.(Strasbourg) - LANDURÉ, JJ.Y.(Brest) LE DREZDEN, E.(Brest) - LEMOIGN, T.(Brest) - LENOBLE, 3 . P. (Paris) - LE SUAVE, R.(Brest) - MEUNIER, 3 . (Brest) PAUTQT, G.(Brest) - REGNAULT, J .P.(Brest) : Nautile submersible dives on deep-sea pelagic deposits in Northeast Central Pacific nodule mining area. /Preliminary ............................ 267 results of Nixonaut cruise/. Xll. CIMBALNIKOVA, A. - ZEMAN, A. (Prague): Sedimentology, mineralogy and petromagnetism of Miocene sediments of Sokolovska Basin /Czechoslovakia/ ................................... 268. GIMENEZ, J. - CALVET, F. (Barcelona): Carbonate dynamics in a deltaic complex from the Southern Pyrenees, Lower Eocene Spain ...................................................... 269. KRIVÂN B. (Budapest): A Lower Cretaceous flsych sequences in the Gerecse Mts. /Hungary/ ............................... 271. SEIFERT, P. (Wien): Sedimentological response on the tectonic development of the Vienna Basin ......................... 273. РОКА T. (Budapest): Complex geochemical method for determination of thermal history ....................................... 275. MARTINI, I.P. (Guelph): Lower Permian coals of Brasil and Quaternary analogs of Canada ............................. 276. FODOR, L., KÀZMÉR, M. (Budapest): Clastic and carbonate sedi mentation in an Eocene strike-slip basin at Budapest .... 277.

(16) p 10th IAS REGIONAL MEETING ON SEDIMENTOLOGY - BUDAPEST, 1989 Use of UJell Logs as a Stratigraphic Tool in Carbonate Series: an example in Southern Iberian Ranges (Spain) ENRIQUE ARACIL Instituto de Geología Económica (CSIC-UCM) SPAIN Continuous core samples are the best tools used in sedimentological ana lysis in subsurface regions. For both technical and economical reasons, the substitutes for coring are well logs. Nowadays well logs are one of the most important tools used by sedimen tologists to know the lithostratigraphy and the geometry of rock units of a shale-sand serie in subsurface studies. However, it is well known that changes in log morphology are difficult to explain in a carbonate serie, because diage netic effects could originate variations in the shape of the curves (Serra, 1973). The purpose of the present work is: (1) to emphasize the importance of qualitative interpretation of continuous well logs as a stratigraphic and sedi mentological tool, and (2) to establish the Cretaceous stratigraphy in Sierra Perenchiza (Perenchiza-1 deep well), unknow because of its lack of outcrops. Lithology was interpreted from the Composite log: G a m m a Ray, Resistivity, Spontaneous Potential, Sonic and Neutron log. Well logs could be divided into several fragments with the same log res ponse tacking into account small breaks in their trends. Two types of "electro sequences" were determined in these fragments: first order sequences, which represent the general trend of a fragment, and second order sequences, which are small variations within first order sequences. The establishment of Lithostratigraphic Units defined by Vilas et al. (1982), was performed from this data. The main application of sequential and li thostratigraphic analysis is the reconstruction of the Cretaceous serie in Sie rra Perenchiza. A field log in Sierra Martes, Giménez (1987), has been used to compare the Upper Cretaceous serie between the vertical profile of Sierra Martes and the well log of Sierra Perenchiza. Both lithology and sequences (1st and 2nd order) are quite similar. On the other hand, thickness of Lithostratigraphic Units also analogous in both series, but in some cases (Margas de Chera For mation, Dolomías de Alatoz Fm., Dolomías Tableadas de Villa de Vés Fm. and Do lomías de la Ciudad Encantada Fm.) the thickness in Perenchiza-1 is 10 per cent smaller than in Sierra Martes. When Composite log quality is good, like in Perenchiza-1 well, and carbona te serie is not anomalous (due to karstification, fracturation, high radiactive minerals content) it is possible to establish Lithostratigraphic Units and first and second order sequences in a well log. By means of the use of well logs, the Cretaceous serie of Sierra Peren chiza has been determined: LJpper Cretaceous is unconfnrmable over Jurassic and its thickness is smaller than Upper Cretaceous in rest of Iberian Ranges because of the situation of Perenchiza-1 well over the Valencian Massif, a pa leogeographic threshold (garcía, 1977)..

(17) ACKNOWLEDGMENTS. The author thanks Dr. Vi las and Dra. Giménez, Facultad de Ciencias Geológicas (Madrid) for their invaluable contribu tions to some aspects about the Upper Cretaceous strati graphy in SUJ Iberian Ranges. BIBLIOGRAPHY GARCIA, A. (1977): Tesis Docto ral. UCM. GIMÉNEZ, R. (1987): Tesis Docto ral. UCM. SERRA, 0. (1973): Bull. Centre Rech. PAU-SNPA, 7, 1, 265-284. VILAS, L., MÁS, J.R., GARCÍA, A ¡ARIAS, C.¡ ALONSO, A.; MELÉN DEZ, N.¡ RINCÓN, R. (1982): In: El Cretácico de España,p: 457509. UCM.. This work has been founded by Dirección General de Investiga ción Científica y Técnica, proyect n: PB033101.. LEGEND 1 : CAL IZAS DE LA BICUERCA MB. 2 : MARGAS DE CHERA FM. 3 : DOLOMÍAS DE ALATOZ FM. 4 : DOLOMÍAS TABLEADAS DE V I LLA DE VES FM. 5 : CAL IZAS Y MARGAS DE CASA MEDINA FM. 6 : DOLOMÍAS DE LA CIUDAD EN CANTADA FM. 7 : MARGAS DE ALARCON FM. 8 :C A LIZA S Y BRECHAS CALCAR^ AS DE SIERRA DE U TIE L FM.. 2. perenchiza -1. s. m a rte s.

(18) P 1 0 th. IA S REGIONAL MEETING ON SEDIMENTOLOGY -. BUDAPEST,. 1989. E a r l y d i a g e n e t i c p r o c e s s e s in l a c u s t r i n e and in re l a t e d flood p l a i n sed i m e n t s fro m the L o w e r C r e t a c e o u s (Central Spain). M. A. A R R IBAS, J.C. GOMEZ FERNANDEZ, & N. MELENDEZ. *Dpto. P e t r o l o g í a y Geoquímica. Fac. CC. Geológicas. 28040 M A D R I D **Dpto. Estrati g r a f í a . Fac. CC. Geológicas. 28040 M A D R I D (SPAIN).. (SPAIN).. Th e L o w e r C r e t a c e o u s of the s o u t h w e s t e r n I b e r i a n Rang e s (Spain), is c h a _ r a c t e r i z e d b y the i n s t a l l a t i o n of m a n y c o n t i n e n t a l systems in a N W - S E o r i e n ted trough, in w h i c h s ome D e p o s i t i o n a l Sequences, c o n t r o l l e d by a t e c t o n i c of bl o c k s w i t h d i f f e r e n t i a l subsidence, w e r e developped. D u r i n g the U p p e r H a u t e r i v i a n - L o w e r Barremian, a w i d e l a c u s t r i n e system, w i t h rela t e d e x t e n s i v e a l l u v i a l - p a l u s t r i n e areas, w a s installed in the stu_ died a rea (east of C u e n c a province, in C e n t r a l Spain). T h e s e d i m e n t o l o g i c a l and p e t r o l o g i c a l study of the c a r b o n a t e facies f r o m the lower C r e t a c e o u s shows a c o n t i n e n t a l diagenesis. Several early s u b a e r i a l d i a g e n e t i c p r o c e s s e s h a v e b e e n di s t i nguished: edaphic b i o t u r b a t i o n due to roots (vertical p r i s m a t i c structures); n o d u l i z a t i o n (at m i c r o s c o p i c a n d m a c r o sc o p i c scale), w i t h c l o t t e d textures and n o d u l a r structures; b r e c c i a t i o n w i t h h o r i z o n t a l and o b l i q u e p l a n a r f issures f o r m a t i o n (skew planes, F R E Y T E T & PLAZIAT, 1982); a n d m a r m o r i z a t i o n . A l l these d i a g e n e t i c pro c e s s e s a r e re lated w i t h a g e n e r a l i z e d p e d o g e n e s i s d e v e l o p m e n t on a p r e v i o u s s e d i m e n t (li mestones, m a r l s or m udstones). Seve r al p e d o g e n e t i c facies h a v e b e e n i d e n t i fied: l i m e s t o n e s w i t h v e r t i c a l p r i s m a t i c s t r u c t u r e s , n o d u l a r l i m e s t o n e s , b r e c c i a t e d l i m e s t o n e s and m a r m o r i z e d l i m e s t o n e s .These p e d o g e n e t i c facies, appea r at the top of l a c u s t r i n e r e t r a c t i o n s e q uences and on flood p l a i n se dimen t s like c a l c i m o r p h i c soils (Fig.), m a r k i n g p h r e a t i c w a t e r - t a b l e f l u c tuations. T h e s u p e r p o s i t i o n of e arly d i a g e n e t i c pr o c e s s e s (pedog e n e t i c pro_ cesses) w i t h i n a p r e v i o u s s e d i m e n t (lacustrine or flood p l a i n de p o s i t s ) is frequ e n t l y found, w h i c h i n d i c a t e lo nger or s h orter periods of s u b a e r i a l e x posure. T h e timing of s u b a e r i a l e x p o s u r e periods (stage of pedogenesis) is a n a l y çed in facies a s s o c i a t i o n s b y abundance, d e v e l o p m e n t and v a r i e t y of p e d o g e n etic processes. T h e s e facies a s s o c i a t i o n s are (Fig.): A) L a c u s t r i n e r e t r a c t i o n s e q u e n c e s w i t h short p eriods of su b a e r i a l e x p o sure. O n l y shows a b i o t u r b a t i o n p r o c esses d e v e l o p e d on l a c u s t r i n e c a r b o n a t e sedim e n t s (vertical p r i s m a t i c structures). B) L a c u s t r i n e r e t r a c t i o n s e q u e n c e s w i t h p r o l o n g a t e d su b a e r i a l exposure, sever a l p e d o g e n e t i c p r o c e s s e s are d e v e l o p e d on l a c u s t r i n e - p a l u s t r i n e c a r b o n a t e sediments, these are: b r e c c i a t i o n , b i o t u r b a t i o n , n o d u l i z a t i o n a n d m a r moriza t i o n . T h e p r o l o n g a t e d s u b a e r i a l e x p o s u r e prod u c e s a stro n g p e d o g e n e sis w i t h h y p e r c a l c i m o r p h i c soil f o r m a t i o n ( p a l e o s o l s ) . C) F l o o d p l a i n s e d i m e n t s (mudstones) w i t h s t a g n a n t w a t e r and p r o l o n g a t e d s u b a e r i a l exposure. A v a r i e t y of p e d o g e n e t i c p r o c e s s e s are d e v e l o p e d o n a p a l u s t r i n e c a r b o n a t e s e d i m e n t fro m the flood p l a i n sediments: b i o t u r b a t i o n , nodu l i z a t i o n , m a r m o r i z a t i o n and bre c ciation. P e d o g e n e s i s is p r o l o n g a t e d and c ont i n u o u s in time, and it p r o d u c e s h i p e r c a l c i m o r p h i c soils (paleosols).. 3.

(19) D) diments smaller d uc e d b y phr e a t i c. N o d u l e s and n o d u l a r c a r b o n a t e levels dev e l o p e d w i t h i n flood p l a i n se (mudstones). In this s u b e n v i r o n m e n t c a l c i u m c a r b o n a t e c o ntent is than in o t h e r o nes (palus trine and lacus t r i n e areas), and it is pro a p u m p i n g e v a p o r a t i o n p r o c e s s e s of c a r bonate rich w a t e r s a b o v e the level.. RE F E R E N C E EREYTET, P. & PLAZIAT, J.C. (1982). C o n t i n e n t a l c a r bonate s e d i m e n t a t i o n and pedogenesis. L a t e C r e t a c e o u s and early T e r t i a r y of south e r n France. C o n t r i b u t i o n s to S e d i m e n t o l o g y , № 1 2 . 21.3 pp.. FLOOD. P L A IN. LACUSTRINE- PALUSTRINE. (STAGNAT AND VADOSE WATER WITH SUBAERIAL EXPOSURE) (WITH SUBAER IA L E X P O S U R E ). L A C U S T R I^ (W ITHOUT. S U B A E R IA L EXPO!. <r D. C. B. A. / IN CR EA SE S U B A ER IA L. OF EXPOSURE. ". ____________ 4. “ ------------------------------^ __________ 4____________________ _CALCIUM C A R B O N A T E C O N T E N T IN SED IMEN TS. ___________________ _____________________________________________________ H IG H E R S U P E R P O S I T I O N OF D IA G EN E TIC PROCESSES. w !. B IO T U R B A T I O N. n. LI M E S T O N E S. n. MUDSTONES. N U U U L I Z A T ION 00’. CAR B O N AT E NODULES. •. M ARM ORIZ ATION. SKEW P L A N E S. 4. MARLS. C H A R O P H YT ES AND OSTRACODES.

(20) 10th IAS REGIONAL MEETING ON SEDIMENTOLOGY - BUDAPEST, 1989 P e t r o l o g y o f the T e r r i g e n o us M i d d l e - U p p e r Alb i a n Series (Basque-Coast, N o r t h e r n Spain) J.M. B A D I L L O - L A R R I E TA * & F. G A R C I A - G A R M I L L A* * * Dpto. E s t ratigrafía, G e o d i n á m i c a y Paleontología. UPV/EHU. 4 8 0 8 0 - B i l b a o (Spain) ** Dpto. M i n e r a l o g í a y Petrología. UPV/EHU. 4 8 0 8 0 - B i l b a o (Spain) The s o - c a l l e d P y r e n e a n Black Fly s c h is largely exposed along the Basque-Coast (Bizkaia and G i p u z k o a Provinces). This s tratigraphic ense m b l e is almost e x c l u s i v e l y c o m p o s e d by terrigenous sediments o f mi d d l e - A l b i a n lower C e n o m a n i a n age. To sum up, it has be e n poss i b l e to d i f f e rentiate several u nits of the B l a c k Fly s c h b e tween E l a ntxobe and Deba towns ( BADI LLO et al., 1988). P e r h a p s there are four of them w h i c h are partic u l a r l y propitious for p e t r o l o g i c studies u nder the micro s c o p e o w i n g to: , a) their g r a i n - s i z e (sandstones and conglomerates) b) their mu t u a l lateral and v e r tical r e l a t i o n s h i p s (chronological and g e o graphical) w h i c h involve s i g n i f i cative age and environmental d i f f e r e n ces. T hese four units are as follows: 1) Name: O n d a r r o a Co n g l o m e r a t e s . Age: middle Albian. Environment: c a nyon/ deep-sea c h a n n e l complex. Lithology: ortho- and paracong l o m e r a te s o f s i liceous c l a s t s up to 35 cm. in diameter. They are composed by quartz, quartzites, silex, s a n d s t o n e and m udstone fragments, siderites and rar e l y calcareous grains. The s a n d s t o n e s (q u a r t z a r e n i t e s , l i t h a r e n i t e s , subl i t h arenites and g raywackes) are c o a r s e - g r a i n e d with normal gradations and siliceous gr a i n s (quartz, v ery f i n e-grained sandstone fragments, silex and quartzites), b u t scarce c a l c a reous compo n e n t s (algal bioclasts and several s p e c i e s o f o r b i t o l i n i d s ). A n other c h a r a c t e r i s t i c features are the presence o f s haly m a t r i x and blocky c a lcite cement. There are also black carbonate p y r i t e - b e a r i n g o r g a n i c - r i c h lutites. 2) Name: L e k e i t i o T u r b i d i t e s and Conglomerates. Age: upper Albian (low part). E n v i r onment: chan n e l system and deep-sea fan. Lithology: s andstones (quartzarenites) ver y s i m i l a r than those of the O n d a r r o a C onglomerates unit, but the b i o c l a s t s and s a n d s t o n e - l i t h oc l a s t s are not frequent. On the o ther han d the a r g i l l a c e o u s mat rix is relat i v e l y rare. The c o n g l o m e r a tes are m a i n l y sil i c e o u s and their g r a i n - s i z e is only about a few cm. Low-carbonate m u d s t o n e s are i l l - r e p resented in this unit. 3) Name: M u t r i k u Sandstones. Age: upper Albian (low part). Environment: d e l t a i c - d i s t r ibu t a r y distal bar. Lithology: f i n e-grained qua r t z - r i c h sandstones (quartzarenites, s u b l i t h arenites and graywackes) with a few bioclasts. The a r g i l l a c e o u s ma t r i x is very frequent and the blocky c a lcite cement is no t uncommon. There are also ca r b o n a t e organi c - r i c h p y ritebearing b lack shales. 4) Name: D e b a T urbidites. Age: upper Albian (late). Environment: deepsea fan. Lithology: well-graded medium-grained siliceous sandstones (litharenites and subli t h a r e n i t e s) compo s e d by quartz, quartzite and s a n d stone fragments, silex and scarce bioclasts. But the more c h a r acteristic.

(21) 1 0 t h IAS R E G I O N A L M E E T I N G ON S E D I M E N T O L O G Y - BUDAPEST, 1989 lith o l o g i c a l feature is the p r e sence o f clasts of volcanic provenance, p a r t i c u l a r l y a b u n d a n t at the u pper part o f the unit. The argillaceous m a trix and the b l o c k y calc i t e c e m e n t are common. Ill-carbonate mudstones are le s s - r i c h in orga n i c m a t t e r and pyrite. The c o m p o s i t i o n a l features of the s t udied units suggest s e d i m e n tary dynam i c s c o n s i s t i n g on h i gh- s u b s i d e n c e rythmic tectodepositional episodes. The a b u n d a n c e o f s e d i m entary and volc a n i c rock-fragments lead us to t hink in at least p e r i o d i c a l l y rapid burial conditions pr o v o k i n g m i n e r a l o g i c a l - i n m a t u r e deposits. On the contrary, the Ondarroa siliceous c o n g l o m e r a t e s are indi c a t i v e o f important r e w o r k i n g processes and thus a r e l e v a n t m i n e r a l o g i c a l maturity.. Cantabrie Sea E la n t x o b e n darroa. B ILB A O. eba. ^SAN. S EB A S TIA N. GEOGRAPHIC LOCATION OF THE TYPE-SECTIO N S. Elantxobe. M IDDLE A LB IA N. Lekeitio Ondarroa Mutriku Deba. O u tc ro p S u rfa ce. ......... CORRELATION SCHEMA SHOWING THE LATERAL AND VERTICAL RELATIONSHIPS BETWEEN THE STUDIED UNITS. 6.

(22) 10th IAS REGIONAL MEETING ON SEDIMENTOLOGY - BUDAPEST,1989 Results of complex sedimentological prospecting of secondary raw materials in Hungary. P.Badinszky - M.Mészáros - Cs. Szabó FTV, Budapest. The round 1 milliard tons of material mass dumped at mine dirt hillocks and on by-product- and waste-heaps in the course of centu ries can be found in about 5 thousand objects in Hungary.. Ihese in. clude the almost total verticum corresponding to the geological struc ture in the form of a heterogeneous mixture. The sedimentological features of the material mixtures are influenced also by the short term geological processes and antropogene effects. Taken into consi deration that an important part of mine dirt hillocks forms seconda ry raw material from the point of view of building, agriculture and environmental protection, therefore their detailed sedimentological prospecting and special geological basic qualification became neces sary. The paper informs about the results gained in the course of ten years of the national prospecting dirested by the Central Geological Office and in the frame of this about the sedimentological classifi cation and qualification resp. of dump materials.. 7.

(23) 1 0th IAS REGIONAL MEETING ON SEDIMENTOLOGY-BUDAPEST ,1989 The Ordovician sediments in the n o r t h e r n P u n a of A r g e n t i n a : C o r r e l a t i o n o f s e d i i n e n to l o g i c , t e c t o n i c and sea level change events HEINRICH BAHLBURG Institut für Geologie und Paläontologie, U n i v e r s i t ä t , E r n s t - R e u t e r - P l a t z 1, 1 0 0 0 B e r l i n 10, FEDERAL REPUBLIC GERMANY.. Technische. In the southern Central Andes of NW Argentina Ordovician e l a s t i c s o c c u r in s h e l f f a c i e s in t h e C o r d i l l e r a O r i e n t a l a n d as basinal turbiditos in the westwardly adjacent Puna highlands. Measurement of d e t a i l e d sections in the n o r t h e r n Puna ( n o r t h of a p p r o x . 2 4 ° 3 0 ’S) a n d n e w f i n d s o f g r a p t o l i t e s led to more precise stratigraphic dating of sedimentary sequences. In the T r e m a d o c i a n , sedimentation in t h e e a s t e r n p a r t of the northern Puna began with a transgressive sequence of quartzarenites and intercalated pebbly mudstones giving way to t u r b i d i t e s . In the w e s t e r n part the oldest fossi1iferous r o c k s o c c u r in the n o r t h C h i l e a n P u n a in the m i d d l e A r e n i g i a n A g u a d a de la P e r d i z F o r m a t i o n . T h i s f o r m a t i o n c o n s i s t s of an approx. 3000 m thick fining upward succession mainly of s u b m a r i n e g r a v i t y m a s s f l o w d e p o s i t s of v o l c a n i c a p r o n f a c i e s . The v o l c a n i c l a s t i c s were d e p o s i t e d on the s u b m a r i n e f l a n k of a zone of mainly subaerial silicic volcanism. Geochemical features of ash flow tuffs and rare basaltic lavas characterize their source as a volcanic arc, which was located west of t h e b a c k - a r c b a s i n . There is' n o e v i d e n c e o f a c t i v e v o l c a n i s m a f ter the A r e n i g i a n . F r o m the late A r e n i g i a n o n w a r d s m i n o r a m o u n t s of b a s e m e n t and sedimentary detritus, derived presumably from the C o r d i l l e r a Oriental, reached the basin together with debris of the volcanic arc. A 700 m thick coarsening upward cycle formed d u r i n g the A r e n i g i a n - L l a n v i r n i a n transition and was probably connected with the initiation of uplift of the Cordillera Oriental (Guandacol diastrophic phase) and tectonic ins tability in the volcanic arc domain to the west. However, tectonic activity and high sedimentation rate at this time c o i ncide w ith a global regre s s i o n event (Fortey, 1004). U pper Llanvirnian and lower L l a n d e i 1 ian turbidites were deposited in a l o n g s t a n d i n g c o m p o s i t e f i n i n g u p w a r d c y ^ d e a l t h o u g h the Cordillera Oriental e m e r g e d in the Lat e L l a n v i r n i a n . Ordovi cian sediments younger than Llanvirnian are not known to o c c u r in the C o r d i l l e r a O r i e n t a l . During the Llandeilian a thick coarsening upward formed which is n o t related to a n y k n o w n , distinct event but is coeval to a world wide regression.. sequence tectonic It was.

(24) succeeded by an even thicker fining upward trend possibly extending into the Caradocian. In the Caradocian the s t r a t i g r a p h i c r e c o r d c o m e s to a n e n d a n d t h e apjjrox . 6 0 0 0 to 7000 m thick basin fill was folded with o u t domin a n t v e r g e n c y in the Ocloyic orogeny during the O r d o v i c i a n - S i 1u r i a n transition. Parallel to these developments, in the Early Caradocian, a e u s t a t i c r i s e in s e a l e v e l t o o k p l a c e w h i c h at the end of the Caradocian and through the Ashgi Ilian gives w a y to a m a j o r w o r l d w i d e r e g r e s s i o n . Immaturity and bad sorting of the turbidite greytvackes in fining upward as well as in coarsening upward megacycles a t t e s t to s h o r t t r a n s p o r t p a t h s a n d m i n o r r e w o r k i n g in s h e l f areas during both cycles. Shelf areas and coastal lowlands were rather small due to u p l i f t of C o r d i l l e r a Oriental and volcanic arc. Sedimentary trends and sea level changes are primarily related to tectonic instability and uplift of source regions induced by active eastward subduct ion under the east Pacific margin of G o n d w a n a . The various global regressions most l ik e ly ^ c o m p l e m e n t e d the influence of tec tonic m o v e m e n t s on d e p o s i t i o n a l patterns.. Ref e rences Fortey, R.A. , 1984, G l o b a l E a r l i e r O r d o v i c i a n t r a n s g r e s s i o n s and regressions and their biological implications: in A s p e c t s of the Ordovician System, ed . D.L. Bruton, Paleontological C o n t r i b u t i o n s f r o m t h e U n i v e r s i t y o f O s l o , v . 2 9 5 , p. 3 7 - 5 0 ..

(25) 10th IAS REGIONAL MEETING ON SEDIMENTOLOGY-BUDAPEST,1989 Cambrian black shale formations of the Siberian platform SERGEY BAKHTUROV Institute of Geology and Geophysics USSR 1. The conditions favourable for the accumulation of the deposits enriched 'by the organic matter appeared more than onse in the sedimentation basins situated in Cambrian on the Siberian platform. In Early Middle Cambrian the ac cumulation of carbonate-argillo-silicon sediments occurred in the north-western, northern and eastern parts of the Siberian platform and in the Yudom-Maysky trough. In Tai myr peninsula and Kharaulalch similar deposits were formed in Upper Cambrian. 2. At present time Kuonamskaya black shale formation combining the deposits of Kuonamskaya, Inikanskaya, Shumninskaya, Sinskaya and the upper past of Sektenskaya sui tes, is the most studied. In the formation composition the argillites enriched by the organic matter, silicon rockes, various limestones and the rockes of mixed composition are widely spread. Its thickness is 40-70m on the average and the estimated area of development is approximately p 750 th. km . The main mineral components of the deposits of Kuonamskaya formation are carbonates, clayey material and authigenous cholcedony. The organic matter often plays the role of the importent rock-forming component - up to 50% in a rock. 3. In Kuonamskaya formation three groups of elements are singled out according to their relation to the orga nic matter: 1) accumulating with the organic matter - Mo, Cd, Bi, V, etc., 2) indifferent to the organic matter Sc, Sn, Be, Zr, etc., 3) antagonistic to the organic mat ter - Nb, Sr, Ba, Y, etc. In Kuonamskaya formation three üevels with the increased phosphate content are established between Kuonamskaya formation and underlying deposits, on.

(26) the base of the formation and in its Amginskaya part. 4. The formation of Kuonamskaya black shale formation takes place within the zone, occupying the intermediate position between a large salt-bearing basin in the south west and the open sea of normal salinity in the east, north-east and north. The reefogenous barrier on one side and isolated areas of land, forming the system of isles, on the other side, were the natural b o u n d a r i e s T h e ac cumulation of sediments, enriched by the organic matter, is caused by two factors: high bioproductivity of the se dimentation basins and existence of anoxic environment of sedimentation. The first is explained by palaeogeographica] specific. features of the Kuonamsky black shale basin.. The second could be caused by two reasons. The existence of stagnant benthic waters could be related to untiestuarive circulation of sea waters to the evaporite basin and to the possible mixtures of waters of increased sali nity with sea waters and their flowing down the bottom of the Kuonamsky basin. In both cases anoxic environments appeared in the benthic part due to water stratification.. 11.

(27) 10th. IAS. REGIONAL. MEETING. ON. SEDIMENTOLOGY. - BUDAPEST,. 1989. Diagenetical history of Dachstein Limestone in the vicinity of Vác. ANNA BALOG. JÄN0S HAAS. Technical University. Central Office of Geology. HUNGARY. HUNGARY. Norian Dachstein Limestone in the vicinity of Vác has been inves tigated with respect to sedimentology, diagenesis, dolomitization and porosity. Carbonates rich in coated grains (ooids, oncoides, grapestones) were accumulated in the high energy outer shelf zone. Due to diagenetical processes took place in several phasis compo sition, texture and porosity of the primary sediments significantly changed as a rule. In the early diagenetic phase carbonate grains were cemented under marine phreatic condition. Due to dissolution of Mg-calcite and arago nite vugs and molds were formed. In the deep burial i.e. anadiagenetic phase pores and cavities were filled by coarse sparite. Dolomitization was partly syndiagenetic but mainly anadiagenetic and could be influenced by hydrothermal processes as well. Dedolomitization and formation of calcific infillings in the fis sures could be taken place in the epidiagenetical phase.. 12. P.

(28) 1Oth IAS REGIONAL MEETING ON SEDIMENTOLOGY - BUDAPEST, 1989 Clay mineraìogy of thè lutites of thè P eraltiìla Formation (Oligocene, NE Spam). BASTIDA, J.*, MAGIAS, I.**, ESTRADA, R. *** & RAMPONE, G. ****. * Opto. Geología. Universidad de Valencia * * I.E.S. Pau Picasso. Terrassa. * * * Dpto Geologìa. U.A.B. * * * * Avda. Verge de Montserrat, 180. Barcelona. The P e ra ltiìla Formation is a succession of Early Oligocene age, cropping-out in the south of the Sierras Marginales that represent the frontal part of the South-central Pyrenees overthrust. Previous studies of facies! Macias 1985, Macias et al. 1986 and Macias et al. in press) have allowed to intepretate the materials of the P eraltiìla Formation as deposits characteristics of the distal front of a wet flu via l fan. The lower part of the stratigraphic succession consists m ainly of sand beds w ith clim bing ripples, included in flood s ilts and lacustrine and palustrine limestones. In the upper part, these materials are not so frequent w hile m ultistorey, lower sinuosity paleochannels appear, increasing the ir size upward. This vertical evolution indicates a progradation of the system, due to the tectonic u p lift of the Sierras Marginales. A selected sampling of the finest materials of the P e raltiìla Formation has been carried out in order to know th e ir m ineralogy. The observed clay mineral assemblages in lutites are: iH ite + chlorite ± kaoiinite. ±. mixed. layer chlorite-sm ectite ± smectite. Quartz, calcite, hematite (± siderite ± gypsum ± p irite ) are present as non clay minerals. Analcime is sometimes found. Illite is the major component of the clay fraction; there are also mixed layer illite -v e rm ic u lite and illite -c h lo rite. Illite and kaoiinite are detrítica! minerals. Chlorite-smectite interlayer content increases when chlorite content decreases so there could be a genetic relation between them because chlorite is a detrítica! but unstable mineral ( Velde, 1985), REFERENCES MACIAS. I. ( 1985).-“Estudi sedimentologie de la Formado Peraltiìla entre Balaguer i Abarras (Provincia de LLeida)". Tesis de ¡.Licenciatura inédita. Universität Autònoma de Barcelona. MACIAS. I., DIAZ MOLINA, M. & ESTRADA, R. (1986) Facies de abanico fluvial en ios afloramientos orientales de la Formación Peraltiìla (Prov. de Lérida). Resúmenes de Comunicaciones. XI Congreso Nacional de Sedimentologia (Barcelona). HACIAS, !., DIAZ MOLINA, M. ', ESTRADA, R. & RAMPONE, 6. (1988) .- "Facies de abanico fluvial en los afloramientos orientales de la Formación Peraltiìla (Prov. de Lérida)“ . Acta Geologica Hispánica un press). VELDE, ß. (1985).- "Clay minerals“ Developments in Sedimentology, 40. Elsevier 427 pp.

(29) 10th IAS REGIONAL MEETING ON SEDIMENTOLOGY - BUDAPEST, 1989. Major erosional discontinuities in the Numidian flysch of Tunisia Bernard BEAUDOIN, Chokri EL MAHERSSI Ecole des Mines de Paris C.G.G.M.-Sédimentologie 35, Rue Saint-Honoré 77305 Fontainebleau cédex FRANCE. The Numidian flysch appears as a Nappe overthrusted on Paleocene and Cretaceous series, from NW to SE, during Upper Miocene. That thick Oligocene-Miocene formation is well exposed along the northern coast of Tunisia and also in land : in all points current directions have been measured by sole marks, indicating a general N —> S orientation (fig. 1). In Sejnane area the sandstone beds influence strongly the morphology : these elongate lenticular bodies are up to 150 m thick, and of hecto-to kilometric length ; they are intercalated in brown shales, and represent less than a quarter of the total thickness (= 3000 m). They are formed by stacked turbiditic and fluxoturbiditic sequences. A first detailed mapping of part of Sejname area allowed to identify more than 50 o f these sandy lenses on a 4 km x 8 km surface ; each one has been followed and characterised in terms of geometry, facies and current direction. After rotation of tectonic dips, correlation and reconstruction of the sedimentary columns by both direct information and geometric reconstructions, a N.NE-S.SW profile may be drawn which concern about 2500 m of sediment along 8 km. The first evidence is that sedimentation was not continuous, but interrupted by successive erosional surfaces which separate sedimentary units.. 14.

(30) wsw. ENE. Two o f these surfaces may be easily drawn : between Aj and B j, and A3/C p Other relations are more hypothetical. These two surfaces present the same characters : the underlying unit is made of horizontal sandy bodies while the overlying one shows smaller bodies dipping southwestward (20 - 30°). When considering the entire succession, two groups of units may be distinguished : in the eastern pan (A }, A 2 , A3) sediments appear horizontal, and current direction is southward ; in the western part (B j, B2, B3 , C j) the sandstone beds are grouped in prograding (westward) systems, dipping also westward, with current directions (sole marks) towards W - S.W : these units are some hundreds meters thick, and some kilometers long. What may represent such an organisation ? These patterns o f erosion (800-1000 m when dccompacted, or more), onlap and progradation during the shaly-sandy turbiditic sedimentation o f the Numidian flysch (Up. Oligocene - L. M iocene) represent major events that may record, in that basin, variations o f sea level. Before correlations at global scale, we have to recognize these erosional discontinuities in other W-Meditcrranean sections and to identify and date the major ones. Nevertheless it gives immediately new guides for the analysis o f that part of the basin..

(31) 10 Th IAS REGIONAL MEETING ON SEDIMENTOLOGY - BUDAPEST, 1989. Bedding and pseudo bedding in alternating limestones and marls : origin and age in Middle Domerian, S. France Bernard BEAUDOIN, Jérôme MAELLART, Daniel MERCIER Ecole des Mines de Paris, C.G.G.M. - Sédimentologie 35, rue Saint-Honoré, 77305 Fontainebleau Cédex FRANCE. The well known "Clue du Vanson" outcrop, E of Sisteron, presents evidences o f Domerian and Toarcian faulting, examples o f active synsedimentary tectonics in that part of the Tethys (fig. la). Precise observation of the Domerian marls leads also to new ideas on the origin of bedding in such type of sediment. A simple description as "marls and interbedded nodular limestones" could not be here sufficient ; the best part of the exposure shows in fact a double system of calcareous nodules (Fig. lb). The first one is roughly parallel to the general bedding : the elements are arranged in rows, but present different sizes and spacing. The second system cut the previous one at high angle (up to 45°) and is made by lines of discontinuous nodules ; moreover the envelops of the nodules sets of the first family are also parallel to the second one. In som e places the similarity between the two networks is such that it is impossible to determine the true bedding.. 16.

(32) I. Following the geometry o f the oblique lines of nodules, it appears that the dip depends of lithology, looking as some refraction : the lowest dip values arc observed in zones devoid in nodules. So that this seems due to differential compaction between the two facies. An hypothesis of plane geometry for the oblique lines leads to a compaction ratio of 1,8 ; decompaction gives then a very simple network for the nodules, disposed according four directions (tectonic dip rotated): horizontal, vertical, two oblique planes at 45°. The last two ones are exactly parallel to the faults in the limy Upper Domerian level (fig. la). All this means that all nodules are diagenctic (bedding and oblique bedding), formed during compaction processes. Calcium carbonate distribution allows to precise the nodulization timing. As often, carbonate content maps present high heterogeneity (fig. 2a) : both nodules and marls show important contrasts, reflecting: -. a continous evolution in nodules along burial, recorded by porosity (carbonate values from 71 % to 44 % correspond to <J>= 63 % up to 29 %, i.e. z from 50 m to 500 m, fig. 2b).. -. "pumping" of CaCOj from marls to nodules, shown by deplcted/halo around the nodules : here also different orientations can be observed, the earliest being rotated by compaction.. Other exposures of the Domerian marls present the same phenomena : it can so be proposed that carbonatation take place along burial, beginning early (some meters or tens o f m.), by an internal migration of carbonate governed by anisotropy o f the sediment, i.e. gravity and cleavages related to tectonics, morphology ... Simple bedding is then a very simple case where only gravity was present..

(33) 10th IAS REGIONAL MEETING ON SEDIMENTOLOGY - BUDAPEST, 1989. Differential mechanical behaviour during diagenesis and compaction in an alternating marl-limestone formation. Bernard BEAUDOIN, Olivier PARITE Ecole des Mines de Paris C.G.G.M.-Sédimentologie 35, Rue Saint-Honoré 77305 Fontainebleau Cédex - FRANCE Numerous sedimentary sandstone sills and dykes cut through shales, slumps and intercalated sandstone beds in some turbiditic formations. They have been studied in the marl-limestone Lower Cretaceous "Blue Marls" (Marnes Bleues) of the Vocontian basin in the western part of the northern margin of the Alpine-Tethys sea. Bevons sections, near Sisteron, South-East o f France (Fig. la), allow to illustrate the "Marnes Bleues" succession (300 meters thick). This pelagic formation is disposed at the top o f the Barremian limestone, occuring upon a lower Aptian discontinuity (hardground, debris flow deposit). Upward it is mainly marly with interbedded slumps and turbidites. The Clansayesian limy beds (Fig. lb , K ) underline the evolution to Albian marls where calcareous beds are more frequent up section ; the very top of Bevons sections is capped by thick channel-filling turbiditic sandstones (Fig. lb). Contemporaneously a complex network of horizontal, oblique and vertical synsedimentary joints was also fossilized by a downward injection from these "in situ" sandy sources. Clastic sills and dykes communicate and so divide the marly massif into blocks.The width of the dykes is usually less than 1 meter but locally may reach 3 meters. Sills may exceed 5 meters in thickness and several hundred meters in lateral extension covering up to tens of square kilometers. The depth o f penetration below this source is o f the order o f 30 meters for the sills and 250 m for the dykes as measured on the Bevons outcrops, without decompaction (Fig. lc).. 78.

(34) Burial o f sediment leads to mechanical compaction with diminution o f initial thickness mostly by lost o f porosity. The dykes are often folded in a ptygmatic fashion, while the sills and some dykes are little deformed and behave as pillars in the series. These occurences allow direct quantification o f the post-injection compaction ratio of the marly sediments which ranges between 1.2 and 2.8. These direct measurements permit to determine the compaction law from the sea-floor to a depth of 400 meters just before the sand injection. Decompaction is necessarily to study clastic dyke geometry i.e. joint geometry at time o f .sand injection (Fig. 2a). Immediatly below the Upper Albian sand-source, i.e. just below the sea-floor, clastic dykes cut through Albian deposits, marl or calcareous shale and limestone, with continuous dip and trend. When they reach a depth of 100 to 150 meters, when they cut through the upper Aptian deposits (Clansaysesian) these dykes underline the marl-limestone contrasts : refractions, dichotomies, differential compaction rates, anastomosis, thickness discontinuities are very frequent (fig. 2b). Some clastic dykes (connected with Upper Albian sand source) cut through Lower Aptian m arls; they are not compacted and fossilized a simple network of vertical and 45° dip joints (fig. lb, c). What does such a vertical evolution reflect ? - Variation o f compaction rate along the first 400 m below sea floor. - Mechanical progressive differentiation with burial between marls and limestone ; one may suggest that this is due to carbonate transfer during diagcnesis/compaction.. 19.

(35) 10th IA S R E G IO N A L M E E T IN G O N S E D IM E N T O L O G Y -B U D A P E S T , 1989. p. Ann Occurence of Badenian Rhyolitic Volcanoclastic R ocks in the Middle Part of Dilj Mountain (Eastern Croatia) M IR K O B E L A K , D A V O R P A V E L lC and M IL K A S A R K O T lC S L A T Institute of Geology, Yugoslavia 41000 Zagreb, Sachsova 2. The aim of the paper is to present datas on sedim entology and petrology of Badenian pyroclastic rocks from Dilj Mt. Polyphase volcanic activity, which took place in the area of Dilj Mt. during the Badenian, controlled paleoenvironmental changes and thus essentally influenced the growth of biolithite bodies. Carbonate rocks with red algaes and/or corals as ree f-fo rm in g orga nism s were deposited during the calm periods. By contrast, the periods of volcanic activity gave rise to a larger influx of volcanoclastic m aterials stop ping the growth of reefs. It is of a particular petrological and sedim entological interest a bed of poorly cemented m onom icte gravel which occurs in lower parts of the lith ostratigra phic colum n Zdenci-I. (bparica et al., 1988). Ve ry sandy conglom eratic bioclastic lim estone grades into poorly cemented m onom ictic gravel. A ll its examined fragm ents and insoluble rezidue of bioclastic limestone (solved in dil. HC1) is of rhyolitic com position. The following rocks were determined: spherulitic rhyolite, aphyric alkali feldspar rhyolite, slightly porphyritic alkali feldspar rhyolite and crystallovitrophyric rhyolitic tuff. The chem ical com position is documented by six chem ical analyses and petro chem ical calculations. They are highly silicic rhyolites characterized by a high content of SiO ^. ranging between 71% and 76%, low content of F e O X, M g O and. C aO and com paratively high content of alkalies, com m only with potassium pre dom inant over sodium. Ve ry sim ilar highly silicic alkali feldspar rhyolites occur in Upper Cretaceous bimodal volcanic association in the neighbouring Poieska gora. M ineral assem blage of rhyolite varieties mentioned above includes: quartz, K feldspar (sanidine-orthoclase), albite, chlorite, sericite and magnetite. Modal mineral com position varies for some sam ples depending on the degree of devitrification of glassy groundmass. in the first published paper dealing with. 20.

(36) 2. Badenian volcanic activity of Dilj Mt. (Pamid et Sparica, 1980) it was em pha sized its synsedim entary character. New additional inform ations on products of Badenian volcanic activity, with the possibility of correlation of some localities, would make possible the explanation of mutual facies relationships in the B a d e nian of northern Croatia and the Pannonian basin, respectively.. References: Pamid, J. & Sparica, M. (1988): Badenian volcanics from Mt. Dilj in Slavonija (N orthern Croatia, Yugoslavia). Bull. Acad. Serbe Scie. natur., 28, 47-56, Beograd.. Sparica, M., Pavelid, D., Miknid, M. & Brkid, M. (1988): M iocene biolithites on Dilj mountain (Slavonia, N orth Croatia). Abstract, Geol. glas., 6, 243-251, Titograd.. 21.

(37) p lOth. IAS. REGIONAL. SEDIMENTOLOGICAL BEACHES. IN. THE. P .B e l l o t t i *,. **. ON. S E D I M E N T O L O G Y - B U D A P E S T ,1989. OF. THE. SURROUNDINGS. OF. ROME,. U . C h i o c c h i m i * *,. *D i p a r t i m e n t o "La. MEETING. CHARACTERS. di. Scienze. PLEISTOCENE. G R A V E L L Y -SANDY. ITALY. N . C i p r i a n i * * * , S. M i l l i *. della. Terra,. Università. di. Roma. S a p i e n z a " , Italy. Facoltà. ***. di. Agraria,. Dipartimento. Università. di. Scienze. Pleistocene. clastic. della. della. Tuscia,. Terra,. Viterbo,. Università. di. Italy. Firenze,. Italy The the. hill. been. area. between. intensively. point sis. of. is. view the. stocene. Ponte. complete Two trend the. physic. to. two. in. the. and. from. a. wave. the. to. as. low. troughs. the. with. coarse. longshore. sandy and. meters. Sands. and. with. thick with. by. bodies. o b 1 i q u e -p 1 a n a r. tinuous. Middle of. a. con. Plei. 40mi t h i c k. and. allowed. to. normal recognize. succession. and. hummocky. rip. along. often. above. phases. sands. with. storm. currents. beds.. contact. interfinger with. an. with. bedding. are. are. filled. lamination. The. whole. lamination. their. is. richer. texturally. of. and. due. to. up. to. and. interpreted sands 15°. storm. ups l o p e , are. omogeneous. Pebbles. are. cha. deposits.. constitute. Sands This. events. phases. in. shows. consist. landwards.. to. medium. sequence. matrix.. decreasing. sand. planes. Erosio-. by. underlying. base. sandy. dipping. probably. acme. the. eros ional. show. inter. events.. downslope. Gravels. abundant. to. gradind■ upwards. laminations of. o b 1 i q u e -p 1 a n a r. gravelly. even. c r o s s - b e d d i n g .S a n d s. alignements. lamination. to. fine. (lower shoreface deposits). ----------------------------------- V m e d i u m - f ine and m e d ium-coarse. setting. become and. analy. deposits. environmental. on. pebbles. Foresets. and. dipping. spheroidal. during. facies. parallel. tangential. lenticular. tively. have. cycle.. geometry. Foresets. gravels. p o s itio n s !. and. consists. (ENE-WSW). decreasing. bars. offlapping. racterized. in. They. chronostratigraphic clastic. roughly. pelites. rare. angle. to. sands. terfingering. coast.. Sici1ian-early which. a. shoreline. connected. to. and. analyzed. l a m i n a t i o n s . The. due. extensively. bottom:. thick. ripples. five. bio. 1ithostratigraphic. as. 22. of. outcrop. tyrrhenian. stratigraphy. The. bioturbation, pebbles. preted. an. the. Formation. quarry. bedding. even. nal. portion. ancient. meters. poor. unknown.. Galeria. following. an. their. but. the. t r a n s g r e s s i v e - r e g r e s s i ve. parallel. 2). from. upper. cuts. (Fig.l) 1). and. studied. practically. stitute. deposits. Rome. of show de. respec. (u p p e r _ s h o -. laterally. con. constitute. thin.

(38) levels. and. fabric wards. show. dipping bg. an. an. oblate. to. prolate. s e a w a r d s . The. erosional. shape. with. whole. sequence. is. with. a pebbly. lag. surface. imbricated truncated. up. (. d e £ O s i t^s j ;. 3). beds. of. medium-coarse. 4m. lying. to. the. cave ve. above. shoreline,. geometry. beds. nels. are. with. Sands. show. The pelites. gravelly. interpreted trend. a parallel. followed. by. beds. longshore. to. the. to. sequence. the. thickness. section to. gravelly. bars. of. normal. even-coneven-conca. filling. rip. chan. shoreline.. o b 1 i q u e -p 1 a n a r. (probable. a. parallel. The. as. with. In. show. base.. 2£ £ : £ £ £ £ _ d £ £ O s i. mentioned. bioturbation. gravels. surface.. erosional. (^££££_£^. above. and. erosional. with. oblique. landwards frequent. the. sands. grades. upwards. foreshore. volcaniclastic. lamination. dipping. ts J .. to. sands. with. and. lagoon. deposits). deposits. of. the. Sabatino. volcanism. The. depos itional. reworking. of. played. important. an. constitutes and/or motif. fluvial a. and role. ravinement. tectonic. event.. characterized. positional phase. setting. which. /mo. motif. by. whole. succession. deposits. by. in. context.. The. this. surface. connected. separates. an. regressive. characterized. recorded. the. deltaic. It a. of. by. fluctuations. a. due. waves.Storm. to. erosional eustatic. underlying. phase. is. from. an. to. events surface. control. depositional overlying. de. tran s g r e s s i v e -regressive. of. the. shoreline.. _ depos its. lagoon. 5 .. deposits. 1. foreshore. upper. deposits. (?). shoreface. depos its ravinement. surface. foreshore. deposits. upper. s h o r e f ace. deposits lower 2-0. .. s h o r e f ace. depos its. Fig.lthe. Log. showing. general. tional. trend. deposi of. grave1 1 y -sandy sits.. the depo.

(39) 10th IAS REGIONAL MEETING ON SEDIMENTOLOGY - BUDAPEST, 1989 Sediment-geological experience of mineral raw material prospecting for the building material industry. Z. Bernath - F. Tarnoczi FTV, Budapest. The FTV Consulting Engineering has been dealing with geological prospecting of raw material for the stone-, gravel-, lime- and cementindustry since more than 30 years. The prospecting results and their modern geostatistical evaluations have indicated several, often sur prising sediment-geological relations. The sediment-geological expe rience could be utilized in the direction of the geological prospec ting. 2Z. work, as well as in the preparation of mining activity..

(40) lOtH IAS REGIONAL MEETING ON SEDIMENTOLOGY. BUDAPEST/ 1989. Lacustrine fan-delta deposits of the Plio-Pleistocene Valdarno Basin, Italy. PAOLO BILLI, MAURIZIO MAGI and MARIO SAGRI University of Florence ITALY The Valdarno is an intermontane basin located 30 Km sout heast of Florence. It has been filled with Middle Pliocene to Pleistocene fluvio-lacustrine deposits belonging to three distinct sedimentary cycles (Abbate, 1983). The first one consists mainly of lacustrine shales ( Middle Pliocene Castelnuovo Group) with interbeds of lignite levels which are indu strially exploited. Such deposits are unconformably overlain by the fluvio-lacustrine sediments of Lower Pleistocene Montevarchi Group which makes up the second cycle and is followed by Middle Pleistocene Monticello Group (Billi et al., 1985). The latter consists of coarse-grained low-sinuosity river deposits (Billi et al., 1987) and represents the third sedi mentary cycle through which the complete infilling of the basin occurred. The basin was bounded by lacustrine fan-delta and alluvial fan systems which gave way to coarse gravel and sand deposits (Pratomagno Group) whose thickness partly re flects the fast uplifting of the basin margins. The fan-delta and the alluvial fan deposits are marginal with respect to those of the second and the third cycle respectively. Object of this presentation is the facies analysis and interpretation of the lacustrine fan-delta deposits. The very proximal subaerial portion is characterized by disorganized, very coarse conglomerates with abundant sandy matrix; the prevailing sedimentary process is mass flow (de bris flood and subordinately debris flow). Downcurrent, such disorganized conglomerates make lateral transition to sequen ces of channellized conglomerates overlain by structureless coarse sand and silt intensely bioturbated and pedogenized. The conglomerate beds are either massive or trough cross-stra tified and generally display distinctive imbrication. They have been interpreted as braided channel deposits. The fan-delta transitional zone is characterized by chan nellized bodies included within massive mud deposits intensely bioturbated and rich in organic matter. The channel fill con sists of trough cross-bedded pebbly sand and massive silt intensely bioturbated and locally pedogenized. Such sediments have been interpreted as deposited by braided distributary channels migrating on a mud flat intermittently subjected to shallow water conditions. The distal, subaqueous portion of the lacustrine fandelta consists of massive mudstone, rich in organic matter, graded or planar cross-laminated sands and channellized, trough cross-laminated pebbly sands arranged in upward thicke.