Geomechanics to Solve Geological Structure Issues: Forward, Inverse and Restoration Modeling Frantz Maerten

Total Page:16

File Type:pdf, Size:1020Kb

Geomechanics to Solve Geological Structure Issues: Forward, Inverse and Restoration Modeling Frantz Maerten Geomechanics to solve geological structure issues: forward, inverse and restoration modeling Frantz Maerten To cite this version: Frantz Maerten. Geomechanics to solve geological structure issues: forward, inverse and restoration modeling. Geophysics [physics.geo-ph]. UNIVERSITE MONTPELLIER II SCIENCES ET TECH- NIQUES DU LANGUEDOC, 2010. English. tel-00537899 HAL Id: tel-00537899 https://tel.archives-ouvertes.fr/tel-00537899 Submitted on 19 Nov 2010 HAL is a multi-disciplinary open access L’archive ouverte pluridisciplinaire HAL, est archive for the deposit and dissemination of sci- destinée au dépôt et à la diffusion de documents entific research documents, whether they are pub- scientifiques de niveau recherche, publiés ou non, lished or not. The documents may come from émanant des établissements d’enseignement et de teaching and research institutions in France or recherche français ou étrangers, des laboratoires abroad, or from public or private research centers. publics ou privés. UNIVERSITE MONTPELLIER II SCIENCES ET TECHNIQUES DU LANGUEDOC THESE pour obtenir le grade de DOCTEUR DE L’UNIVERSITE MONTPELLIER II Discipline : Structure et ´evolution de la lithosph`ere Ecole doctorale : SIBAGHE pr´esent´ee et soutenue publiquement par Frantz MAERTEN Le 17 juin 2010 Titre : Geomechanics to solve geological structure issues: forward, inverse and restoration modeling JURY: M. Jean Ch´ery U. Montpellier, France Directeur de th`ese M. David D. Pollard U. Stanford, USA Codirecteur de th`ese M. Bruno L´evy INRIA,France Rapporteur M. Yves Leroy ENS Paris, France Rapporteur M. Xavier Legrand Repsol,Madrid Examinateur M. Marc Daigni`eres U. Montpellier, France Examinateur RESUM´ E´ Utilisation de la g´eom´ecanique pour r´esoudre des probl`emes li´es aux structures g´eologiques: mod´elisation directe, inversion et restauration Diff´erentes applications de l’´elasticit´elin´eaire en g´eologie structurale sont pr´esent´ees dans cette th`ese `atravers le d´eveloppement de trois types de codes num´eriques. Le premier utilise la mod´elisation directe pour ´etudier les d´eplacements et champs de contraintes au- tour de zones faill´ees complexes. On montre que l’ajout de contraintes in´egalitaires, telles que la friction de Coulomb, permet d’expliquer l’angle d’initiation des dominos dans les re- lais extensifs. L’ajout de mat´eriaux h´et´erog`enes et d’optimisations, telles la parall´elisation sur processeurs multi-cœurs ainsi que la r´eduction de complexit´edes mod`eles, permettent l’´etude de mod`eles beaucoup plus complexes. Le second type de code num´erique utilise la mod´elisation inverse, aussi appel´ee estimation de param`etres. L’inversion lin´eaire de d´eplacements sur les failles ainsi que la d´etermination de pal´eo-contraintes utilisant une approche g´eom´ecanique sont d´evelopp´ees. Le dernier type de code num´erique concerne la restauration de structures complexes pliss´es et faill´ees. Il est notamment montr´equ’une telle m´ethode permet de v´erifier l’´equilibre de coupes g´eologiques, ainsi que de retrouver la chronologie des failles. Finalement, nous montrons que ce mˆeme code permet de lisser des horizons 3D faill´es, pliss´es et bruit´es en utilisant la g´eom´ecanique. MOTS-CLES:´ G´eologie structurale, ´elasticit´elin´eaire, mod´elisation directe, inversion, restauration 1 ABSTRACT Geomechanics to solve geological structure issues: forward, inverse and restoration modeling Different applications of linear elasticity in structural geology are presented in this the- sis through the development of three types of numerical computer codes. The first one uses forward modeling to study displacement and perturbed stress fields around com- plexly faulted regions. We show that incorporating inequality constraints, such as static Coulomb friction, enables one to explain the angle of initiation of jogs in extensional relays. Adding heterogeneous material properties and optimizations, such as paralleliza- tion on multicore architectures and complexity reduction, admits more complex models. The second type deals with inverse modeling, also called parameter estimation. Linear slip inversion on faults with complex geometry, as well as paleo-stress inversion using a geomechanical approach, are developed. The last type of numerical computer code is dedicated to restoration of complexly folded and faulted structures. It is shown that this technique enables one to check balanced cross-sections, and also to retrieve fault chronol- ogy. Finally, we show that this code allows one to smooth noisy 3D interpreted faulted and folded horizons using geomechanics. KEYWORDS: Structural geology, linear elasticity, forward modeling, inverse modeling, restoration modeling 2 “Imagination is more important than knowledge” Albert Einstein 3 Preface This thesis is comprised of work that started a while ago, when I was unemployed after a bachelor degree in geophysics and geology at the University of Montpellier II. It has been continued at Stanford University within the research group of Pr David D. Pollard for four years, mainly on correcting, rewriting, enhancing and optimizing an existing 3D boundary element code. Then, several publications have emerged while at Igeoss, a start-up that we created in 2004 in Montpellier with my brother Laurent (who did his PhD with Pr David Pollard), and David Pollard himself. After my return to France from Stanford to start Igeoss, the idea of doing a PhD came to my mind when I realized that a VAE (”valorisation des acquis et de l’experience” which can be translated to ”appreciation of achievements and experiences”) was now possible in France to obtain the equivalent of a master degree in order to start a PhD. Marc Daigni`eres, a professor at the University of Montpellier II, successfully supported my request against a faculty commitee and I was able to start in November 2006, under the direction of Jean Chery (France) and Dave Pollard (USA). Walking in the world of geomechanics, numerical methods, optimizations and program- ming without any knowledge and background is not so simple, but can lead to new insights with the help of the imagination (hence the quote of this thesis). Eleven papers are pre- sented and one is in the appendix, which show the usefulness of linear elasticity. Although during this period three other papers were published (see appendix C), I do not include them within this thesis as I was only a little bit involved. I particularly show in this thesis that using the simple conceptual model of linear elasticity can lead to many application codes which are used to better understand geological struc- tures using either forward, inverse or restoration modeling. The large number of publica- tions using such codes by researchers around the world (more than one hundred twenty), demonstrates their importance. A complete list of publications in different geological do- mains can be obtained on the Igeoss support website at https://support.igeoss.com. Doing this thesis was the opportunity to start the company Igeoss in 2004 in Montpellier, and to continue the research on iBem3D, Dynel2D and Dynel3D while giving 13 inter- national conferences and writing 11 papers as well as a patent for the estimation of the state of stress in complex reservoirs using measures from well bores and faults geometry. 4 Finally, Igeoss integrated Schlumberger, the world’s leading supplier of technology in the oil and gas industry worldwide, after the acquisition in April 2010. 5 Acknowledgments I wish to thanks, first, Dave Pollard who gently guided me in the comprehension of structural geology and geomechanics while at Stanford University. He accepted to take me in his Rock Fracture Project (RFP) group while I was programming graphical interfaces in a small company in Montpellier, and without any knowledge in numerical codes and geomechanics. I think that his choice was mainly motivated by the fact that (1) Laurent, my brother, was already working with him as a ’very good’ PhD student, and that (2) during my free time in France, I was coding a new numerical code in 2D and 3D, namely Dynel. My brother Laurent is also greatly acknowledged, and it is still a pleasure to work together: him, the structural geologist, and me the analytical geologist. While at Stanford University (USA) and in Montpellier (FRANCE), I met many stu- dents, researchers and people from the industry who provided me a diversity of view- points in the domains of structural geology, geophysics and computer sciences. They include (alphabetical ordered): Fabrizio Agosta, Marco Antonellini, Atilla Aydin, Taixu Bai, Loic Bazalgette, Nicolas Bellahsen, Stephan Bergbauer, Stephan Bourne, Jean Ch´ery, Michele Cooke, Juliet Crider, Marc Daigni`eres, Nick Davatzes, Russell Davies, Guil- laume Deconchy, Guilhen De Joussineau, Xavier Du-Bernard, Peter Eichhubl, Patricia Fiore, Eric Flodin, Juan Mauricio Florez, Paul Gillespie, Radu Girbacea, Brita Gra- ham, Paul Griffiths, Joel Ita, Herv´eJourde, Simon Kattenhorn, Ole Kaven, Sotiris Kokkalas, S´ebatien Lacase Serge Lallemand, Xavier Legrand, Bruno Levy, Lidia Lon- ergan, Michel Lopez, Peter Lovely, Stephen Martel, Maurice Mattauer, Matteo Molinaro, Jordan Muller, Ovunc Multu, Rodrick Myers, Ian Mynatt, Fabien Pauget, Jean-Pierre Pe- tit, Jean-Christophe Perez, Phil Resor, Paul Segall, Michel Seranne, Roger Soliva, Kurt 6 Sternlof, Lans Taylor, Haiquing Wu, Scott Young, Amgad Younes, Wenbing Zhang, Marc Zoback, and certainly many other people... I thanks people who accepted to review this work in a short time: Bruno Levy and Yves
Recommended publications
  • Introduction San Andreas Fault: an Overview
    Introduction This volume is a general geology field guide to the San Andreas Fault in the San Francisco Bay Area. The first section provides a brief overview of the San Andreas Fault in context to regional California geology, the Bay Area, and earthquake history with emphasis of the section of the fault that ruptured in the Great San Francisco Earthquake of 1906. This first section also contains information useful for discussion and making field observations associated with fault- related landforms, landslides and mass-wasting features, and the plant ecology in the study region. The second section contains field trips and recommended hikes on public lands in the Santa Cruz Mountains, along the San Mateo Coast, and at Point Reyes National Seashore. These trips provide access to the San Andreas Fault and associated faults, and to significant rock exposures and landforms in the vicinity. Note that more stops are provided in each of the sections than might be possible to visit in a day. The extra material is intended to provide optional choices to visit in a region with a wealth of natural resources, and to support discussions and provide information about additional field exploration in the Santa Cruz Mountains region. An early version of the guidebook was used in conjunction with the Pacific SEPM 2004 Fall Field Trip. Selected references provide a more technical and exhaustive overview of the fault system and geology in this field area; for instance, see USGS Professional Paper 1550-E (Wells, 2004). San Andreas Fault: An Overview The catastrophe caused by the 1906 earthquake in the San Francisco region started the study of earthquakes and California geology in earnest.
    [Show full text]
  • Monoclinal Flexure of an Orogenic Plateau Margin During Subduction, South Turkey
    Non-peer reviewed preprint submitted to EarthArXiv Monoclinal flexure of an orogenic plateau margin during subduction, south Turkey Running title: Monoclinal flexure plateau margin David Fernández-Blanco1, Giovanni Bertotti2, Ali Aksu3 and Jeremy Hall3 1Tectonics and Structural Geology Department, Faculty of Earth and Life Sciences, Vrije Universiteit Amsterdam, De Boelelaan 1085, 1081 HV Amsterdam, the Netherlands [email protected] 2Department of Geotechnology, Faculty of Civil Engineering and Geosciences, Delft University of Technology, Stevinweg 1, 2628CN, Delft, the Netherlands 3 Department of Earth Sciences, Centre for Earth Resources Research, Memorial University of Newfoundland, St. John's, Newfoundland, Canada A1B 3X5 Non-peer reviewed preprint submitted to EarthArXiv Abstract Geologic evidence across orogenic plateau margins helps to discriminate the relative contributions of orogenic, epeirogenic and/or climatic processes leading to growth and maintenance of orogenic plateaus and plateau margins. Here, we discuss the mode of formation of the southern margin of the Central Anatolian Plateau (SCAP), and evaluate its time of formation, using fieldwork in the onshore and seismic reflection data in the offshore. In the onshore, uplifted Miocene rocks in a dip-slope topography show monocline flexure over >100 km, few-km asymmetric folds verging south, and outcrop- scale syn-sedimentary reverse faults. On the Turkish shelf, vertical faults transect the basal latest Messinian of a ~10 km fold where on-structure syntectonic wedges and synsedimentary unconformities indicate pre-Pliocene uplift and erosion followed by Pliocene and younger deformation. Collectively, Miocene rocks delineate a flexural monocline at plateau margin scale, expressed along our on-offshore sections as a kink- band fold with a steep flank ~20–25 km long.
    [Show full text]
  • Lesson 3 Forces That Build the Land Main Idea
    Lesson 3 Forces That Build the Land Main Idea Many landforms result from changes and movements in Earth’s crust. Objectives Identify types of landforms and the processes that form them. Describe what happens when an earthquake occurs. Vocabulary fault focus aftershock seismic wave epicenter seismograph magnitude vent What forces change Earth’s crust? At transform boundaries, the pieces of rock rub together in a force called shearing, like the blades of a pair of scissors, causing the rock to break. At convergent boundaries, plates collide and this force is called compression, squeezing the rock together. At divergent boundaries, plates separate causing tension, making the crust longer and thinner eventually breaking and creating a fault. Faults are usually located along the boundaries between tectonic plates. Three Kinds of Faults Shearing forms strike-slip faults. Tension forms normal faults. The rock above the fault moves down. Compression forms reverse faults. The rock above the fault moves up. Uplifted Landforms Folded mountains are mostly made up of rock layers folded by being squeezed together. Fault-block mountains are made by huge, tilted blocks of rock separated from the surrounding rock by faults. The Colorado Plateau was formed when rock layers were pushed upward. The Colorado River eventually formed the Grand Canyon. Quick Check Infer Why are faults often produced along plate boundaries? Forces act on the crust most directly at plate boundaries, because these locations are where plates are moving, relative to each other. Critical Thinking Why do some mountains form as folded mountains and others form as fault-block mountains? Compression forces form folded mountains, and tension forms fault- block mountains.
    [Show full text]
  • Structural Modeling Based on Sequential Restoration of Gravitational Salt Deformation in the Santos Basin (Brazil)
    Marine and Petroleum Geology xxx (2012) 1e17 Contents lists available at SciVerse ScienceDirect Marine and Petroleum Geology journal homepage: www.elsevier.com/locate/marpetgeo Structural modeling based on sequential restoration of gravitational salt deformation in the Santos Basin (Brazil) Sávio Francis de Melo Garcia a,*, Jean Letouzey b, Jean-Luc Rudkiewicz b, André Danderfer Filho c, Dominique Frizon de Lamotte d a Petrobras E&P-EXP, Rio de Janeiro, Brazil b IFP Energies Nouvelles, France c Universidade Federal de Ouro Preto, Ouro Preto/MG, Brazil d Université de Cergy-Pontoise, France article info abstract Article history: The structural restoration of two parallel cross-sections in the central portion of the Santos Basin enables Received 8 December 2010 a first understanding of existent 3D geological complexities. Santos Basin is one of the most proliferous Received in revised form basins along the South Atlantic Brazilian margin. Due to the halokinesis, geological structures present 22 November 2011 significant horizontal tectonic transport. The two geological cross-sections extend from the continental shelf Accepted 2 February 2012 to deep waters, in areas where salt tectonics is simple enough to be solved by 2D restoration. Such cross- Available online xxx sections display both extensional and compressional deformation. Paleobathymetry, isostatic regional compensation, salt volume control and overall aspects related to structural style were used to constrain basic Keywords: fl Salt tectonics boundary conditions. Several restoration
    [Show full text]
  • Part 3: Normal Faults and Extensional Tectonics
    12.113 Structural Geology Part 3: Normal faults and extensional tectonics Fall 2005 Contents 1 Reading assignment 1 2 Growth strata 1 3 Models of extensional faults 2 3.1 Listric faults . 2 3.2 Planar, rotating fault arrays . 2 3.3 Stratigraphic signature of normal faults and extension . 2 3.4 Core complexes . 6 4 Slides 7 1 Reading assignment Read Chapter 5. 2 Growth strata Although not particular to normal faults, relative uplift and subsidence on either side of a surface breaking fault leads to predictable patterns of erosion and sedi­ mentation. Sediments will fill the available space created by slip on a fault. Not only do the characteristic patterns of stratal thickening or thinning tell you about the 1 Figure 1: Model for a simple, planar fault style of faulting, but by dating the sediments, you can tell the age of the fault (since sediments were deposited during faulting) as well as the slip rates on the fault. 3 Models of extensional faults The simplest model of a normal fault is a planar fault that does not change its dip with depth. Such a fault does not accommodate much extension. (Figure 1) 3.1 Listric faults A listric fault is a fault which shallows with depth. Compared to a simple planar model, such a fault accommodates a considerably greater amount of extension for the same amount of slip. Characteristics of listric faults are that, in order to maintain geometric compatibility, beds in the hanging wall have to rotate and dip towards the fault. Commonly, listric faults involve a number of en echelon faults that sole into a low­angle master detachment.
    [Show full text]
  • Kinematics of the Northern Walker Lane: an Incipient Transform Fault Along the Pacific–North American Plate Boundary
    Kinematics of the northern Walker Lane: An incipient transform fault along the Paci®c±North American plate boundary James E. Faulds Christopher D. Henry Nevada Bureau of Mines and Geology, MS 178, University of Nevada, Reno, Nevada 89557, USA Nicholas H. Hinz ABSTRACT GEOLOGIC SETTING In the western Great Basin of North America, a system of dextral faults accommodates As western North America has evolved 15%±25% of the Paci®c±North American plate motion. The northern Walker Lane in from a convergent to a transform margin in northwest Nevada and northeast California occupies the northern terminus of this system. the past 30 m.y., the northern Walker Lane has This young evolving part of the plate boundary offers insight into how strike-slip fault undergone widespread volcanism and tecto- systems develop and may re¯ect the birth of a transform fault. A belt of overlapping, left- nism. Tertiary volcanic strata include 31±23 stepping dextral faults dominates the northern Walker Lane. Offset segments of a W- Ma ash-¯ow tuffs associated with the south- trending Oligocene paleovalley suggest ;20±30 km of cumulative dextral slip beginning ward-migrating ``ignimbrite ¯are up,'' 22±5 ca. 9±3 Ma. The inferred long-term slip rate of ;2±10 mm/yr is compatible with global Ma calc-alkaline intermediate-composition positioning system observations of the current strain ®eld. We interpret the left-stepping rocks related to the ancestral Cascade arc, and faults as macroscopic Riedel shears developing above a nascent lithospheric-scale trans- 13 Ma to present bimodal rocks linked to Ba- form fault.
    [Show full text]
  • Tectonic Evolution of Structures in Southern Sindh Monocline, Indus Basin, Pakistan Formed in Multi-Extensional Tectonic Episodes of Indian Plate
    Tectonic Evolution of Structures in Southern Sindh Monocline, Indus Basin, Pakistan Formed in Multi-Extensional Tectonic Episodes of Indian Plate Sarfraz Hussain Solangi, Shabeer Ahmed, Muhammad Akram Qureshi, Mohammad Shahid, Uzair Hamid Awan Universityof Sindh, Pakistan Summary There are number of structures and structural styles found in extensional tectonic settings of the world but the evolution of these structuresis still needful and a big challenge as well. Evolution of structures in extensional settings have been studied by Yuan Li et al., (2016)and many other reserachers on different extensional basins of the world. Sindh Monocline lies on the western corner of Indian Plate and the tectonic history of Indian plate has been well described by Chatterjee et al., (2013) while tectonic history of Sindh Monocline has been studied by Zaigham, and Mallick, (2000), Chatterjee et al., (2013) (Fig.1). The aim of this study is the evolution of structures in the subsurface of Southern Sindh Monocline, Pakistan using the seismic data interpretation and faltenning of horizons approach. Jamaluddin et al., (2015) and others have also testified such approach. Southern Sindh Monocline is charaterized and experienced by different tectonic episodes of Indian plate while rifting from Gondwanaland, rifting from other plates at different geological times and to its collision with the Asia. Basic structures with in study area are classified into nine types whilethe structural styles have been classified into six types as horst and grabens,dominos,crotch,synthetic
    [Show full text]
  • Late Mesozoic Compressional to Extensional Tectonics in The
    Late Mesozoic compressional to extensional tectonics in the Yiwulüshan massif, NE China and its bearing on the evolution of the Yinshan-Yanshan orogenic belt: Part I: Structural analyses and geochronological constraints Wei Lin, Michel Faure, Yan Chen, Wenbin Ji, Fei Wang, Lin Wu, Nicolas Charles, Jun Wang, Qingchen Wang To cite this version: Wei Lin, Michel Faure, Yan Chen, Wenbin Ji, Fei Wang, et al.. Late Mesozoic compressional to extensional tectonics in the Yiwulüshan massif, NE China and its bearing on the evolution of the Yinshan-Yanshan orogenic belt: Part I: Structural analyses and geochronological constraints. Gond- wana Research, Elsevier, 2013, 23 (1), pp.54-77. 10.1016/j.gr.2012.02.013. insu-00681290 HAL Id: insu-00681290 https://hal-insu.archives-ouvertes.fr/insu-00681290 Submitted on 21 Aug 2012 HAL is a multi-disciplinary open access L’archive ouverte pluridisciplinaire HAL, est archive for the deposit and dissemination of sci- destinée au dépôt et à la diffusion de documents entific research documents, whether they are pub- scientifiques de niveau recherche, publiés ou non, lished or not. The documents may come from émanant des établissements d’enseignement et de teaching and research institutions in France or recherche français ou étrangers, des laboratoires abroad, or from public or private research centers. publics ou privés. Late Mesozoic compressional to extensional tectonics in the Yiwulüshan massif, NE China and its bearing on the evolution of the Yinshan–Yanshan orogenic belt: Part I: Structural analyses and geochronological constraints Wei Lina Michel Faureb Yan Chenb Wenbin Jia Fei Wanga Lin Wua Nicolas Charlesb Jun Wanga Qingchen Wanga a State Key Laboratory of Lithospheric Evolution, Institute of Geology and Geophysics, Chinese Academy of Sciences, P.O.
    [Show full text]
  • Describe the Geometry of a Fault (1) Orientation of the Plane (Strike and Dip) (2) Slip Vector
    Learning goals - January 16, 2012 You will understand how to: Describe the geometry of a fault (1) orientation of the plane (strike and dip) (2) slip vector Understand concept of slip rate and how it is estimated Describe faults (the above plus some jargon weʼll need) Categories of Faults (EOSC 110 version) “Normal” fault “Thrust” or “reverse” fault “Strike-slip” or “transform” faults Two kinds of strike-slip faults Right-lateral Left-lateral (dextral) (sinistral) Stand with your feet on either side of the fault. Which side comes toward you when the fault slips? Another way to tell: stand on one side of the fault looking toward it. Which way does the block on the other side move? Right-lateral Left-lateral (dextral) (sinistral) 1992 M 7.4 Landers, California Earthquake rupture (SCEC) Describing the fault geometry: fault plane orientation How do you usually describe a plane (with lines)? In geology, we choose these two lines to be: • strike • dip strike dip • strike is the azimuth of the line where the fault plane intersects the horizontal plane. Measured clockwise from N. • dip is the angle with respect to the horizontal of the line of steepest descent (perpendic. to strike) (a ball would roll down it). strike “60°” dip “30° (to the SE)” Profile view, as often shown on block diagrams strike 30° “hanging wall” “footwall” 0° N Map view Profile view 90° W E 270° S 180° Strike? Dip? 45° 45° Map view Profile view Strike? Dip? 0° 135° Indicating direction of slip quantitatively: the slip vector footwall • let’s define the slip direction (vector)
    [Show full text]
  • Systematic Variation of Late Pleistocene Fault Scarp Height in the Teton Range, Wyoming, USA: Variable Fault Slip Rates Or Variable GEOSPHERE; V
    Research Paper THEMED ISSUE: Cenozoic Tectonics, Magmatism, and Stratigraphy of the Snake River Plain–Yellowstone Region and Adjacent Areas GEOSPHERE Systematic variation of Late Pleistocene fault scarp height in the Teton Range, Wyoming, USA: Variable fault slip rates or variable GEOSPHERE; v. 13, no. 2 landform ages? doi:10.1130/GES01320.1 Glenn D. Thackray and Amie E. Staley* 8 figures; 1 supplemental file Department of Geosciences, Idaho State University, 921 South 8th Avenue, Pocatello, Idaho 83209, USA CORRESPONDENCE: thacglen@ isu .edu ABSTRACT ously and repeatedly to climate shifts in multiple valleys, they create multi­ CITATION: Thackray, G.D., and Staley, A.E., 2017, ple isochronous markers for evaluation of spatial and temporal variation of Systematic variation of Late Pleistocene fault scarp height in the Teton Range, Wyoming, USA: Variable Fault scarps of strongly varying height cut glacial and alluvial sequences fault motion (Gillespie and Molnar, 1995; McCalpin, 1996; Howle et al., 2012; fault slip rates or variable landform ages?: Geosphere, mantling the faulted front of the Teton Range (western USA). Scarp heights Thackray et al., 2013). v. 13, no. 2, p. 287–300, doi:10.1130/GES01320.1. vary from 11.2 to 37.6 m and are systematically higher on geomorphically older In some cases, faults of known slip rate can also be used to evaluate ages landforms. Fault scarps cutting a deglacial surface, known from cosmogenic of glacial and alluvial sequences. However, this process is hampered by spatial Received 26 January 2016 Revision received 22 November 2016 radionuclide exposure dating to immediately postdate 14.7 ± 1.1 ka, average and temporal variability of offset along individual faults and fault segments Accepted 13 January 2017 12.0 m in height, and yield an average postglacial offset rate of 0.82 ± 0.13 (e.g., Z.
    [Show full text]
  • The Role of Pressure Solution Seam and Joint Assemblages In
    THE ROLE OF PRESSURE SOLUTION SEAM AND JOINT ASSEMBLAGES IN THE FORMATION OF STRIKE-SLIP AND THRUST FAULTS IN A COMPRESSIVE TECTONIC SETTING; THE VARISCAN OF SOUTHWESTERN IRELAND Filippo Nenna and Atilla Aydin Department of Geological and Environmental Sciences, Stanford University, Stanford, CA 94305 e-mail: [email protected] scale such as strike-slip faults and thrust-cored folds in Abstract various stages of their development. In this study we focus on the initiation and development of strike-slip The Ross Sandstone in County Clare, Ireland, was faults by shearing of the initial JVs and PSSs and deformed by an approximately north-south compression formation of thrust faults by exploiting weak shale during the end-Carboniferous Variscan orogeny. horizons and the strike-parallel PSSs in the adjacent Orthogonal sets of fundamental structures form the sandstone intervals. initial assemblage; mutually abutting arrays of 170˚ Development of faults from shearing of initial oriented set 1 joints/veins (JVs) and approximately 75˚ fundamental structural elements with either opening or pressure solution seams (PSSs) that formed under the closing modes in a wide range of structural settings has same stress conditions. Orientations of set 2 (splay) JVs been extensively reported. Segall and Pollard (1983), and PSSs suggest a clockwise remote stress rotation of Martel and Pollard (1989) and Martel (1990) have about 35˚ responsible for the contemporaneous described strike-slip faults formed by shearing of shearing of the set 1 arrays. Prominent strike-slip faults thermal fractures in granitic rocks. Myers and Aydin are sub-parallel to set 1 JVs and form by the linkage of (2004) and Flodin and Aydin (2004) reported strike-slip en-echelon segments with broad damage zones faulting formed by shearing of joints formed by an responsible for strike-slip offsets of hundreds of metres.
    [Show full text]
  • Structural and Metamorphic Investigation of the Cathedral Rock – Drew Hill Area, Olary Domain, South Australia
    STRUCTURAL AND METAMORPHIC INVESTIGATION OF THE CATHEDRAL ROCK – DREW HILL AREA, OLARY DOMAIN, SOUTH AUSTRALIA. Jonathan Clark (B.Sc.) Department of Geology and Geophysics University of Adelaide This thesis is submitted as a partial fulfilment for the Honours Degree of a Bachelor of Science November 1999 Australian National Grid Reference (SI 54-2) 1:250 000 i ABSTRACT The Cathedral Rock – Drew Hill area represents a typical Proterozoic high-grade gneiss terrain, and provides an excellent basis for the study of the structural and metamorphic geology in early earth history. Rocks from this are comprised of Willyama Supergroup metasediments, which have been subjected to polydeformation. The highly strained nature of the area has been attributed to three deformations. These have been superimposed into a single structure, the Cathedral Rock synform, which represents a second-generation fold that refolds the F1 axial surface. Pervasive deformation with a northwest transport direction firstly resulted in the formation of a thin-skinned duplex terrain. Crustal thickening in the middle to lower crust led to the reactivation of basement normal faults in a reverse sense. Further compression, led to more intense folding and thrusting associated with the later part of the Olarian Orogeny. Strain analysis has shown that the region of greatest strain occurs between the Cathedral Rock and Drew Hill shear zones. Cross section restoration showed that this area has undergone approximately 65% shortening. Further analysis showed that strain fluctuated across the area and was affected by the competence of different lithologies and the degree of recrystallisation. ii Contents Abstract (ii) List of Plates, Tables and Figures (v) Acknowledgments (vi) CHAPTER 1:INTRODUCTION 1 1.1.
    [Show full text]