Northern Carnarvon Basin Locality Map
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1 PATTERNS of MONTOYA GROUP DEPOSITION, DIAGENESIS, and RESERVOIR DEVELOPMENT in the PERMIAN BASIN Rebecca H. Jones ABSTRACT
PATTERNS OF MONTOYA GROUP DEPOSITION, DIAGENESIS, AND RESERVOIR DEVELOPMENT IN THE PERMIAN BASIN Rebecca H. Jones ABSTRACT Rocks composing both the Montoya (Upper Ordovician) and Fusselman (Lower Silurian) Formations were deposited during the global climate transition from greenhouse conditions to unusually short-lived icehouse conditions on a broad, shallow-water platform. The Montoya and the Fusselman also share many reservoir characteristics and have historically been grouped together in terms of production and plays. Recently, however, the Montoya has garnered attention on its own, with new gas production in the Permian Basin and increased interest in global Ordovician climate. Recent outcrop work has yielded new lithologic and biostratigraphic constraints and an interpretation of four third-order Montoya sequences within Sloss’s second-order Tippecanoe I sequence. The Montoya Group comprises the Upham, Aleman, and Cutter Formations, from oldest to youngest. The Upham contains a basal, irregularly present sandstone member called the Cable Canyon. The boundary between the Montoya and the Fusselman is readily definable where a thin shale called the Sylvan is present but can be difficult to discern where the Sylvan is absent. Montoya rocks were deposited from the latest Chatfieldian to the end of the Richmondian stage of the late Mohawkian and Cincinnatian series (North American) of the Upper Ordovician. Montoya reservoir quality is generally better in the northern part of the Permian Basin where it is primarily dolomite compared to limestone Montoya reservoirs in the south. Reservoir quality is also better in the lower part of the unit compared to the upper, owing to a predominance of porous and permeable subtidal ooid grainstones and skeletal packstones in the former and peritidal facies in the latter. -
48. Laboratory-Determined Sound Velocity
48. LABORATORY-DETERMINED SOUND VELOCITY, POROSITY, WET-BULK DENSITY, ACOUSTIC IMPEDANCE, ACOUSTIC ANISOTROPY, AND REFLECTION COEFFICIENTS FOR CRETACEOUS-JURASSIC TURBIDITE SEQUENCES AT DEEP SEA DRILLING PROJECT SITES 370 AND 416 OFF THE COAST OF MOROCCO1 Robert E. Boyce, Deep Sea Drilling Project, Scripps Institution of Oceanography, La Jolla, California ABSTRACT From 661 to 880 m beneath the seafloor at DSDP Sites 370 and 416 are Albian to Barremian claystone with some limestone, sandstone, and siltstone. Compressional-wave velocities ranged from 1.70 to 4.37 km/s, with an average in situ vertical velocity of 1.93 km/s. From 880 to 1430 m are Hauterivian to Valanginian turbidites of alternating graded calcareous and quartzose cycles from siltstone or fine sandstone to mudstone. Compressional-wave velocities range from 1.80 to 4.96 km/s with an average in situ velocity of 2.61 km/s. From 1430 to 1624 m are early Valanginian to Tithonian (Kimmeridgian?) turbidites, with alternating quartzose silt- stone grading to mudstone cycles with hard micritic limestone and calcarenite (calciturbidites). Compressional-wave velocities range from 2.26 to 5.7 km/s, with an average in situ vertical velocity of 3.25 km/s. Acoustic anisotropy is 0 to 30% faster parallel to bedding in Cretaceous to Tithonian sandstone-siltstone turbidites in mudstone and minor limestone from 661 to 1624 m below the seafloor. Between 2.0(?) km/s and 4.2(?) km/s, anisot- ropy becomes particularly significant (below 1178 m), where the anisotropy is about +0.4 km/s or greater. The mud- stone, softer sandstone, and softer siltstone tend to have velocities around 2.0 to 2.5 km/s; the cemented sandstone and limestone cluster around 2.5 km/s to 4.2 km/s; thus the relative percentage anisotropy is greater for lower-velocity li- thologies. -
Depositional Environments
trast the Kunrade Chalk occupies a smaller area The depositional environments of the Maastricht outcrop in the northeast corner of South Limburg between Valken- and Kunrade Chalks (Maastrichtian) from the burg and Heerlen - extending also into West Germany. type area of Limburg, Netherlands Lithofacies: R.E. Pollock by The Maastricht and Kunrade Chalks are essentially calca- of reous, with a varying amount terrigenous clastic con- ABSTRACT: tent which is more evident in the Kunrade Chalk. We Following the deposition of the Gulpen Chalk ICampanian-Maas- the two ‘chalks’ their trichlianl. the Maastricht and Kunrade Chalks exhibit typicalfeate- can split up on, firstly outcrop pat- shallow carbonate There and their res of high energy water deposition. is a tern, on their lithology, finally on depositional progressive shallowing through the depositionof the Maastricht Chalk environments. as typifiedby the changes from calcilutite Ichalk I deposition in the The contemporaneity of these two deposits has in the past lower Maastricht Chalk to medium and coarse grained calcarenities been in but it is fairly well documented that the with occasional calcirudites in the higher levels. This trend is paral- dispute Kunrade Chalk is lateral the leled in the faunal characteristics, exhibiting an increase in abun- a equivalent of Maastricht dance and diversity of the benthos. Chalk In the between (Romein, 1963). area Valkenburg and Kunrade the Maastricht and Kunrade Chalks can be Introduction: seen to interfinger (Kruit, 1949). the Following widespread trangression during the Upper The of these chalks from calcisiltites lithologies range with its in the late and Cretaceous peak Campanian early and calcarenites containing subordinate terrigenous clas- Maastrichtian, there followed over most of Northwest tic horizons in the Kunrade Chalk to medium to coarse with the of the Europe a regional regression deposition calcarenites and calcirudites in the Maastricht Chalk. -
Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey)
Open Geosci. 2015; 7:446–464 Research Article Open Access Murat Gül* Occurrences of Chert in Jurassic-Cretaceous Calciturbidites (SW Turkey) DOI 10.1515/geo-2015-0029 ubility controls silica precipitation, it increases with tem- perature and pH values (especially pH>9) [2]. Received November 25, 2013; accepted February 20, 2015 Chert can be deposited via organic and inorganic path- Abstract: The Lycian Nappes, containing ophiolite and ways [3]. Silica-secreting organisms play an important sedimentary rocks sequences, crop out in the southwest role in organic chert deposition and silica precipitation, Turkey. The Tavas Nappe is a part of the Lycian Nappes. in water undersaturated with silica [2]. These organisms It includes the Lower Jurassic-Upper Cretaceous calcitur- are the radiolarians, diatoms, silicoagellates and opa- bidites. Chert occurrences were observed in the lower part line silica-shelled microplankton [2]. Many studies have of this calciturbidite. These cherts can be classied on the focused on these organisms, especially on the radiolar- basis of length, internal structure and host rock. Chert ians [4–6]. The inorganic chert formation requires over- bands are 3.20-35.0 m in length and 7.0-35.0 cm thick. Chert saturated solutions with silica and silica replacement [3]. lenses are 5.0-175.0 cm in length and 1.0-33.0 cm thick. Ac- The silica may be sourced from rivers, mid-ocean ridge vol- cording to its internal structure, granular chert (bladed- canic products that reacted with sea water, and silica par- large equitant quartz minerals replaced the big calcite ticles on the sea oor [2]. -
(Ordovician) of Central Kentucky
Lithostratigraphy and Depositional Environments of the Lexington Limestone (Ordovician) of Central Kentucky By EARLE R. CRESSMAN GEOLOGICAL SURVEY PROFESSIONAL PAPER 768 Prepared in cooperation with the Kentucky Geological Survey A desc1·ijJtion of a Middle and UpjJer Ordovician limestone formation and its constituent members with a discussion of facies 1·elations) environn~ents of dejJosition) and jxlleogeography UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON 1973 UNITED STATES DEPARTMENT OF THE INTERIOR 'ROGERS C. B. MORTON, Secretary GEOLOGICAL SURVEY V. E. McKelvey,. Director Library of Congress catalog-card No. 73-600094 For sale by the Superintendent of Documents, U.S. Government Printing Office Washington, D.C. 20402. Price: paper cases-$8. 70, domestic postpaid; $8.25, GPO Bookstore Stock Number 2401-00362 . CONTENTS Page Page Abstract ---------------------------------------- 1 Stratigraphy-Continued Introduction ------------------------------------- 1 Lexington Limestone-Continued Geologic setting ____ - _--- ____ --_------------------ 8 Devils Hollow Member ------------------ 40 11 Millersburg Member --------------------- 41 Stratigraphy ------------------------------------ 44 11 Clays Ferry Formation ---------------------- Lexington Limestone ------------------------- 45 Curdsville Limestone Member ____ _: _______ _ 11 Kope Formation ---------------------------- Point Pleasant Formation -------------------- 46 15 Logana Member ------------------------ Fauna ----------------------------------------- 46 Grier Limestone -
University Microfilms, Inc., Ann Arbor, Michigan the UNIVERSITY of OKLAHOMA
This dissertation has been 66—1871 microfilmed exactly as received GLASER, Gerald Clement, 1936- LITHOSTRATIGRAPHY AND CARBONATE PETROLOGY OF THE VIOLA GROUP (ORDO VICIAN), ARBUCKLE MOUNTAINS, SOUTH- CENTRAL OKLAHOMA. The University of Oklahoma, Ph.D., 1966 Geology University Microfilms, Inc., Ann Arbor, Michigan THE UNIVERSITY OF OKLAHOMA GRADUATE COLLEGE LITHOSTRATIGRAPHY AND CARBONATE PETROLOGY OF THE VIOLA GROUP (ORDOVICIAN), ARBUCKLE MOUNTAINS, SOUTH-CENTRAL OKLAHOMA A DISSERTATION SUBMITTED TO THE GRADUATE FACULTY in partial fulfillment of the requirements for the degree of DOCTOR OF PHILOSOPHY BY GERALD CLEMENT GLASER Norman, Oklahoma 1965 LITHOSTRATIGKAPHÏ AND CARBONATE PETROLOGY OF THE VIOLA GROUP (ORDOVICIAN), ARBUCKLE MOUNTAINS, SOUTH-CENTRAL OKLAHOMA APPRO DISSERTATION COMMITTEE ACKNOWLEDGMENTS This study is submitted in partial fulfillment of the requirements for the degree of Doctor of Philosophy at The University of Oklahoma. The problem was directed by Dr. C. J. Mankin whose advice and supervision are gratefully acknowledged. I am particularly grateful to Dr. W. E. Ham of the Oklahoma Geological Survey•for his help both with the carbon ate rocks and the lithostratigraphic problems associated with this work. Besides reading “die manuscript, he has uhecked the field work, made innumerable helpful suggestions, stimu lated many thought-provoking discussions, and has made avail able to the writer data on chemical analyses of some of the limestones. Special thanks are due Drs. C. C. Branson and P. K. Sutherland for their critical appraisal of the manuscript and the suggestions offered by them for its improvement. The writer wishes to thank the National Science Foundation for providing funds for the preparation of thin iii sections and other services connected with this work; the Oklahoma Geological Survey for helping to defray field ex penses ; and Mr. -
Depositional Setting of the Sedimentary Rocks Contai
ZOBODAT - www.zobodat.at Zoologisch-Botanische Datenbank/Zoological-Botanical Database Digitale Literatur/Digital Literature Zeitschrift/Journal: Veröffentlichungen des Tiroler Landesmuseums Ferdinandeum Jahr/Year: 2006 Band/Volume: 86 Autor(en)/Author(s): Sanders Diethard, Ostermann Marc-André Artikel/Article: Depositional setting of the sedimentary rocks containing the "warm-interglacial" fossil flora of the Höttinger Brekzie (Pleistocene, Northern Calcareous Alps, Austria): a reconstruction. 91-118 © Tiroler Landesmuseum Ferdinandeum, Innsbruck download unter www.biologiezentrum.at Veröffentlichungen des Tiroler Landesmuseums Ferdinandeum 86/2006 Innsbruck 2006 91-118 Depositional setting of the sedimentary rocks contai- ning the "warm-interglacial" fossil flora of the Höttin- ger Brekzie (Pleistocene, Northern Calcareous Alps, Austria): a reconstruetion Diethard Sanders & Marc Ostermann Ablagerungsraum der Sedimentgesteine mit der „warm-interglazialen" Flora der Höttinger Brekzie (Pleisto- zän, Nördliche Kalkalpen, Österreich): eine Rekonstruktion Abstraft Most of Ihe plants fossils of a reputed, "warm-interglacial" flora of the Höttinger Brekzie ncar Innsbruck (Pleistoce- nc, Northern Calcareous Alps) were deposited in a shallow pond, or ephemeral ponds, that were affected by episo- dic debris flows and mudflows. The fossiliferous section at about 1110-1130 m a.s.l. at "Rossfall-Lahner" is traditionally assigned to the Höttinger Brekzie, a lithified succession deposited mainly from stream-dominated alluvial fans and from talus slopes. The Höt- tinger Brekzie aecumulated after the Riss Glacial and lithified well-before the Last Glacial Maximum. At Rossfall- Lahner, the rock Substrate is represented by Triassic red beds and carbonates. At present. the fossiliferous interval is largely covered by Vegetation, hence its depositional setting was reconstrueted from fossil collections, field mapping, and from a tailing. -
The Engineering Geological Characterisation of the Barzaman Formation, with Reference to Coastal Dubai, UAE
The Engineering Geological Characterisation of the Barzaman Formation, with reference to Coastal Dubai, UAE Steve Macklin Associate Director, Arup Geotechnics, London e-mail: [email protected] Richard Ellison Regional Manager, British Geological Survey Jason Manning Senior Geologist, Arup Geotechnics, London Andrew Farrant Geologist, British Geological Survey Leon Lorenti Senior Geotechnical Engineer, Arup Pty Ltd, Perth Abstract This paper describes, from field exposures, temporary excavations and borehole core, the pedogenically altered fluvial deposits found in the UAE termed the Barzaman Formation. This formation comprises a sequence of rocks dominated by variably cemented conglomerates thought to be middle Miocene to Pliocene in age. The sequence is interpreted as an alluvial fan succession (or “bajada”) laid down in response to uplift and erosion of the Hajar Mountains. A ground model for this formation is described to explain the distinct lithological features of the formation, comprising terrestrial fluvial and alluvial plain deposits that have been modified by cementation and dolomitisation, duricrust formation and pedogenic processes during arid periods over repeated climatic cycles. Four principle lithologies thus typically occur as a rhythmic alternation of a basal conglomerate (composed predominantly of clasts of ophiolite and chert) overlain by an irregular bed of white conglomerate and “calcisiltite” and passing upwards into a pale grey to green clay and siltstone “breccia”. The white conglomerate and calcisiltite largely represent deposits of dolomite-palygorskite duricrust. The well established Clarke & Walker (1979) descriptive scheme currently used for describing the formation is reviewed and a simple visual descriptive lithological classification proposed. The classification is described in terms of the three principal lithological components visible in hand specimen: mottled white calcisiltite matrix/cement, palygorskite rich marl and clasts derived from the Oman Mountains (gabbro, chert and weathered ultramafic rock). -
18. Turbidite Facies, Associations, and Sequences in the Southeastern Angola Basin1
18. TURBIDITE FACIES, ASSOCIATIONS, AND SEQUENCES IN THE SOUTHEASTERN ANGOLA BASIN1 Dorrik A. V. Stow, Grant Institute of Geology, University of Edinburgh, Edinburgh, Scotland, EH9 3JW, United Kingdom ABSTRACT Turbidite sedimentation occurred throughout the Cretaceous to Recent history of the Angola Basin but was particu- larly important in three discrete intervals of fan development. Three turbidite classes are identified: classical sandy tur- bidites (both volcanogenic and calcarenite types); silt and mud turbidites (including five types based on Stow turbidite divisions); and biogenic turbidites (both pelagic and calcilutite types). These various turbidites are best described and in- terpreted in terms of two related turbidite models (Bouma, 1962; Stow, 1977). Complete and partial sequences of each model can be interpreted in terms of depositional process and subenvironment. The composition of the sediment (sand, mud, biogenic, terrigenous, etc.) is found to play an important part in the nature of turbidites deposited. Vertical facies sequences on the sandy volcanogenic "green fan" are interpreted as channel, lobe, and basin plain environments. For the muddy biogenic "brown fan," inner and outer fan and basin plain environments are more ap- propriate. Characteristic facies associations for each of these settings are described, based on facies types and propor- tions, turbidite frequency, bed thickness, grain size, and sedimentary structures. These associations are characteristic of open-ocean deep-water fans and basin plains and are significantly different from those described from land-based studies of ancient fans in small, more shallow-water, tectonically active basins. INTRODUCTION CLASSICAL SANDY TURBIDITES The sediment pile cored at Deep Sea Drilling Project These turbidites occur in both the green and white (DSDP) Site 530 in the S.E. -
Part I. Montoya and Related Colonial Corals. Part II. Organisms Attached
MEMOIR 7 PART I Montoya and Related Colonial Corals PART II Organisms Attached to Montoya Corals By ROUSSEAU H. FLOWER TEXT SECTION STATE BU REAU OF MINES AND MINERAL RESOU RCES NEW MEXICO INSTITUTE OF MINING AND TECHNOLOGY CAMPUS STATION SOCORRO, NEW MEXICO NEW MEXICO INSTITUTE OF MINING & TECHNOLOGY E. J. Workman, President STATE BUREAU OF MINES AND MINERAL RESOURCES Alvin J. Thompson, Director THE REGENTS MEMBERS Ex OFFICIO The Honorable Edwin L. Mechem Governor of New Mexico Tom Wiley . ... Superintendent of Public Instruction APPOINTED MEMBERS William G. Abbott .... Hobbs Holm 0. Bursum, Jr. .Socorro Thomas M. Cramer .. .. Carlsbad Frank C. DiLuzio . ............ Albuquerque Eva M. Larrazolo (Mrs. Paul F.). .. Albuquerque Published November 21, 1961 For Sale by the New Mexico Bureau of Mines & Mineral Resources Campus Station, Socorro, N. Mex.-$4.00. Price includes text and plate sections. Contents PART I MONTOYA AND RELATED COLONIAL CORALS Page ABSTRACT 3 INTRODUCTION 3 ACKNOWLEDGMENTS. 6 THE MONTOYA GROUP . 7 General divisions and correlations . 7 Harding-Winnipeg remnants IO The Second Value formation I I Aleman formation 13 Cutter formation 13 FAUNAL ANALYSIS 14 I. The Montoya group 14 II. Western and northern Ordovician faunas . 15 Burnam limestone . 15 Maravillas chert 15 Arizona 15 Colorado 15 Bighorn region 15 British Columbia .. 15 Winnipeg region 16 Red River formation . 16 Stony Mountain formation . 16 Stonewall formation 16 Hudson Bay .. 16 Nelson limestone . 16 Shamattawa limestone 16 Akpatok Island 16 Baffin Island 17 Cape Calhoun region 17 Gonioceras Bay formation 18 Cape Calhoun formation 18 Scattered Arctice occurrences . 18 III. Eastern North America 18 Lake St. -
Petrology and Weathering Environment of Sub-Unconformity
University of Arkansas, Fayetteville ScholarWorks@UARK Theses and Dissertations 5-2015 Petrology and Weathering Environment of Sub- unconformity Limestone unit: The Kessler Limestone member of the Bloyd Formation, Morrowan (Pennsylvanian) Northwest Arkansas Thomas Daniels Dolan University of Arkansas, Fayetteville Follow this and additional works at: http://scholarworks.uark.edu/etd Part of the Geology Commons Recommended Citation Dolan, Thomas Daniels, "Petrology and Weathering Environment of Sub-unconformity Limestone unit: The Kessler Limestone member of the Bloyd Formation, Morrowan (Pennsylvanian) Northwest Arkansas" (2015). Theses and Dissertations. 8. http://scholarworks.uark.edu/etd/8 This Thesis is brought to you for free and open access by ScholarWorks@UARK. It has been accepted for inclusion in Theses and Dissertations by an authorized administrator of ScholarWorks@UARK. For more information, please contact [email protected], [email protected]. Petrology and Weathering Environment of sub-unconformity limestone unit: The Kessler Limestone Member of the Bloyd Formation, Morrowan (Pennsylvanian) Northwest Arkansas Petrology and Weathering Environment of sub-unconformity limestone unit: The Kessler Limestone Member of the Bloyd Formation, Morrowan (Pennsylvanian) Northwest Arkansas A thesis submitted in partial fulfillment of the requirements for the degree of Master of Science in Geology by Thomas D. Dolan University of Arkansas Bachelor of Science in Earth Science, 2012 May 2015 University of Arkansas This Thesis is approved for recommendation to the Graduate Council. ________________________________________ Dr. Doy Zachry Thesis Director ________________________________________ ____________________________________ Dr. Matt Covington Dr. Chris Liner Committee Member Committee Member ABSTRACT In northwest Arkansas the thin, widespread Pennsylvanian Kessler Limestone of the Bloyd Formation is exposed in numerous locations. -
Cedar Valley Formation (Devonian) of Minnesota and Northern Iowa
MINNESOTA GEOLOGICAL SURVEY MATT S. WALTON, Director CEDAR VALLEY FORMATION (DEVONIAN) OF MINNESOTA AND NORTHERN IOWA John H. Mossier I5il Report of Investigations 18 UNIVERSITY OF MINNESOTA Saint Paul . 1978 CEDAR VALLEY FORMATION {DEVONIAN} OF MINNESOTA AND NORTHERN IOWA CONTENTS Page Abstract Introduction 2 Stratigraphy 5 solon Member 5 Basal biogenic dolostone facies 5 Dolomitic calcilutite facies •• 7 Upper biogenic dolostone facies 7 Rapid Member • • • • • • • • • • • • • • • • • • 9 Basal massive argillaceous dolostone facies • 9 Upper laminated argillaceous dolostone facies 9 Coralville Member. 11 Basal biogenic dolostone facies • • • • • • • 11 Lower sparsely fossiliferous dolostone facies 12 Lower pelletal calcilutite facies • • • • • • 12 Upper sparsely fossiliferous dolostone facies 14 Upper pelletal calcilutite facies. • • • • • • • • 14 Stromatoporoid biostrome facies. • • • • • • • • • 16 Upper contact of the Cedar Valley Formation 16 Shale partings in the Cedar Valley Formation • • • • • • • 17 Paleoenvironmental interpretation • • • • • • • • • • • • • • • 17 Solon Member • • • • • • • • • • • • • • • • • • • • • • • 18 Rapid Member • • • • • • • • • • • • • • • • • • • • 18 Coralville Member. • • • • • • • • 18 Dolomitization and other diagenetic alterations • • • • • • • 19 Recognition of the Cedar Valley Formation and its members in the subsurface. • • • • • • • 21 Economic geology •••••••••••••••••••••••• 23 Acknowledgments • • • • • • • • • • • • • • • • • • • • • • • • 23 References cited. 24 Appendix A Cedar Valley