MECHANICAL ENGINEERING Syllabus
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Preliminary Structural Study of the Gold-Bearing Shear Zone System at the Seabee Mine, Northern Saskatchewan
Preliminary Structural Study of the Gold-bearing Shear Zone System at the Seabee Mine, Northern Saskatchewan Ghislain Tourigny Tourigny, G. (2003): Preliminary structural study of the gold-bearing shear zone system at the Seabee Mine, northern Saskatchewan; in Summary of Investigations 2003, Volume 2, Saskatchewan Geological Survey, Sask. Industry Resources, Misc. Rep. 2003-4.2, CD-ROM, Paper B-1, 11p. Abstract The Seabee gold deposit is a structurally controlled, mesothermal vein gold deposit developed in weakly deformed metagabbroic rocks of the Laonil Lake Intrusive Complex, northern Saskatchewan. The gold-bearing veins are hosted by narrow, steeply northwest-dipping to subvertical, northeast- and east-northeast-trending shear zones consisting of well-foliated L-S tectonites that are characterized by a steep mylonitic foliation and a steeply west- plunging mineral lineation. Auriferous veins occur as riedel ‘R’ and ‘P’ veins oriented 5° to 15° from the shear foliation, as fault-fill veins subparallel to the foliation, and as minor extension veins oriented at a high angle to the shear zone boundary. Coexisting strain and kinematic indicators reveal that the auriferous shear zones recorded a strong component of boundary-normal compression combined with subhorizontal dextral shear. The auriferous shear zones are either late reverse faults, reactivated as dextral strike-slip faults, or dextral transpression zones developed between converging rigid walls. Preliminary interpretation suggests that dextral transpression best explains the emplacement and deformation of the shear zones and associated gold-quartz veins. Keywords: Seabee mine, Laonil Lake Intrusive Complex, gold mineralization, shear zone, C-S fabric, foliation, reverse faults, transpression, dextral shear, deformation partitioning. -
Faults and Ductile Shear Zones) from Selected Drill Cores P-07-227
Oskarshamn site investigation – Structural characterization of deformation zones (faults and ductile shear zones) from selected drill cores site investigation – Structural characterization Oskarshamn P-07-227 Oskarshamn site investigation Structural characterization of deformation zones (faults and ductile shear zones) from selected drill cores and outcrops from the Laxemar area – Results from Phase 2 Giulio Viola, Guri Venvik Ganerød Geological Survey of Norway, Trondheim, Norway December 2007 Svensk Kärnbränslehantering AB Swedish Nuclear Fuel and Waste Management Co Box 250, SE-101 24 Stockholm Tel +46 8 459 84 00 P-07-227 CM Gruppen AB, Bromma, 2008 ISSN 1651-4416 Tänd ett lager: SKB P-07-227 P, R eller TR. Oskarshamn site investigation Structural characterization of deformation zones (faults and ductile shear zones) from selected drill cores and outcrops from the Laxemar area – Results from Phase 2 Giulio Viola, Guri Venvik Ganerød Geological Survey of Norway, Trondheim, Norway December 2007 Keywords: Oskarshamn, AP PS 400-06-098, Structural geology, Shear zone, Fault, Fault rocks, Kinematics. This report concerns a study which was conducted for SKB. The conclusions and viewpoints presented in the report are those of the authors and do not necessarily coincide with those of the client. Data in SKB’s database can be changed for different reasons. Minor changes in SKB’s database will not necessarily result in a revised report. Data revisions may also be presented as supplements, available at www.skb.se. A pdf version of this document can be downloaded from www.skb.se. Abstract A study of predominantly brittle structures, i.e. brittle deformation zones, faults, fractures and associated fault rocks, was carried out on a number of drill cores and outcrops of the Laxemar area, Oskarshamn. -
Deformation Characteristics of the Shear Zone and Movement of Block Stones in Soil–Rock Mixtures Based on Large-Sized Shear Test
applied sciences Article Deformation Characteristics of the Shear Zone and Movement of Block Stones in Soil–Rock Mixtures Based on Large-Sized Shear Test Zhiqing Li 1,2,3,*, Feng Hu 1,2,3, Shengwen Qi 1,2,3, Ruilin Hu 1,2,3, Yingxin Zhou 4 and Yawei Bai 5 1 Key Laboratory of Shale Gas and Geoengineering, Institute of Geology and Geophysics, Chinese Academy of Sciences, Beijing 100029, China; [email protected] (F.H.); [email protected] (S.Q.); [email protected] (R.H.) 2 College of Earth and Planetary Science, University of Chinese Academy of Sciences, Beijing 100049, China 3 Innovation Academy of Earth Science, Chinese Academy of Sciences, Beijing 100029, China 4 Yunnan Chuyao Expressway Construction Headquarters, Chuxiong 675000, China; [email protected] 5 Henan Yaoluanxi Expressway Construction Co. LTD, Luanchuan 471521, China; [email protected] * Correspondence: [email protected] or [email protected]; Tel.: +86-13671264387 Received: 27 July 2020; Accepted: 15 September 2020; Published: 17 September 2020 Abstract: Soil–rock mixtures (SRM) have the characteristics of distinct heterogeneity and an obvious structural effect, which make their physical and mechanical properties very complex. This study aimed to investigate the deformation properties and failure mode of the shear zone as well as the movement of block stones in SRM experimentally, not only considering SRM shear strength. The particle composition and proportion of specimens were based on field samples from an SRM slope along national highway 318 in Xigaze, Tibet. Shear zone deformation tests were carried out using an SRM-1000 large-sized geotechnical apparatus controlled by a motor servo, considering the effects of different stone contents by mass (0, 30%, 50%, 70%), vertical pressures (50, 100, 200, 300, and 400 kPa), and block stone sizes (9.5–19.0, 19.0–31.5, and 31.5–53.0 mm). -
Faults and Joints
133 JOINTS Joints (also termed extensional fractures) are planes of separation on which no or undetectable shear displacement has taken place. The two walls of the resulting tiny opening typically remain in tight (matching) contact. Joints may result from regional tectonics (i.e. the compressive stresses in front of a mountain belt), folding (due to curvature of bedding), faulting, or internal stress release during uplift or cooling. They often form under high fluid pressure (i.e. low effective stress), perpendicular to the smallest principal stress. The aperture of a joint is the space between its two walls measured perpendicularly to the mean plane. Apertures can be open (resulting in permeability enhancement) or occluded by mineral cement (resulting in permeability reduction). A joint with a large aperture (> few mm) is a fissure. The mechanical layer thickness of the deforming rock controls joint growth. If present in sufficient number, open joints may provide adequate porosity and permeability such that an otherwise impermeable rock may become a productive fractured reservoir. In quarrying, the largest block size depends on joint frequency; abundant fractures are desirable for quarrying crushed rock and gravel. Joint sets and systems Joints are ubiquitous features of rock exposures and often form families of straight to curviplanar fractures typically perpendicular to the layer boundaries in sedimentary rocks. A set is a group of joints with similar orientation and morphology. Several sets usually occur at the same place with no apparent interaction, giving exposures a blocky or fragmented appearance. Two or more sets of joints present together in an exposure compose a joint system. -
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) -
Pressure Solution and Hydraulic Fracturing by a Lastair Beach
C H E M !C A L P R O C E S S E S IN D E F O R M A T IO N A T L O W M E T A M O R P H IC G R A D E S Pressure Solution and Hydraulic Fracturing by A lastair Beach Pressure solution has long been recognized as an im portant m echanism of de和rm ation, particularly in sedim entary rocks at low m etam orphic grade. G eologists have tended to study only the m ost easily m anaged aspect of pressure solution structures 一their geom etry as a record of rock deform ation. A t the sam e tim e the m ost co m m on pressure solution structures, such as stylolites in lim estones, clearly evolve th rough com plex chem ical processes, as do cleavage stripes and associa ted syntectonic veins w hich are abundant in terrigenous sedim entary rocks that have been d e form ed under lo w grade m etam orphic conditions. This review 和cusses on stripes and veins, draw ing together those concepts that need integrated study in o rd e r to r e a c h a b e t te r understanding a厂pressure solution. G eological Setting s m a lle r s c a le in s la t e s a n d t h e d e fin it io n o f c h e m ic a l a n d m ineralogical changes associated w ith cleavage developm ent Spaced cleavage stripes are the w idespread result of defor- (K nipe, 1982). -
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. -
Sedimentary Stylolite Networks and Connectivity in Limestone
Sedimentary stylolite networks and connectivity in Limestone: Large-scale field observations and implications for structure evolution Leehee Laronne Ben-Itzhak, Einat Aharonov, Ziv Karcz, Maor Kaduri, Renaud Toussaint To cite this version: Leehee Laronne Ben-Itzhak, Einat Aharonov, Ziv Karcz, Maor Kaduri, Renaud Toussaint. Sed- imentary stylolite networks and connectivity in Limestone: Large-scale field observations and implications for structure evolution. Journal of Structural Geology, Elsevier, 2014, pp.online first. <10.1016/j.jsg.2014.02.010>. <hal-00961075v2> HAL Id: hal-00961075 https://hal.archives-ouvertes.fr/hal-00961075v2 Submitted on 19 Mar 2014 HAL is a multi-disciplinary open access L'archive ouverte pluridisciplinaire HAL, est archive for the deposit and dissemination of sci- destin´eeau d´ep^otet `ala diffusion de documents entific research documents, whether they are pub- scientifiques de niveau recherche, publi´esou non, lished or not. The documents may come from ´emanant des ´etablissements d'enseignement et de teaching and research institutions in France or recherche fran¸caisou ´etrangers,des laboratoires abroad, or from public or private research centers. publics ou priv´es. 1 2 Sedimentary stylolite networks and connectivity in 3 Limestone: Large-scale field observations and 4 implications for structure evolution 5 6 Laronne Ben-Itzhak L.1, Aharonov E.1, Karcz Z.2,*, 7 Kaduri M.1,** and Toussaint R.3,4 8 9 1 Institute of Earth Sciences, The Hebrew University, Jerusalem, 91904, Israel 10 2 ExxonMobil Upstream Research Company, Houston TX, 77027, U.S.A 11 3 Institut de Physique du Globe de Strasbourg, University of Strasbourg/EOST, CNRS, 5 rue 12 Descartes, F-67084 Strasbourg Cedex, France. -
Deformation in Moffat Shale Detachment Zones in the Western Part of the Scottish Southern Uplands
This is a repository copy of Deformation in Moffat Shale detachment zones in the western part of the Scottish Southern Uplands. White Rose Research Online URL for this paper: http://eprints.whiterose.ac.uk/1246/ Article: Needham, D.T. (2004) Deformation in Moffat Shale detachment zones in the western part of the Scottish Southern Uplands. Geological Magazine, 141 (4). pp. 441-453. ISSN 0016-7568 https://doi.org/10.1017/S0016756804009203 Reuse See Attached Takedown If you consider content in White Rose Research Online to be in breach of UK law, please notify us by emailing [email protected] including the URL of the record and the reason for the withdrawal request. [email protected] https://eprints.whiterose.ac.uk/ Geol. Mag. 141 (4), 2004, pp. 441–453. c 2004 Cambridge University Press 441 DOI: 10.1017/S0016756804009203 Printed in the United Kingdom Deformation in Moffat Shale detachment zones in the western part of the Scottish Southern Uplands D. T. NEEDHAM* Rock Deformation Research, School of Earth Sciences, The University, Leeds LS2 9JT, UK (Received 17 June 2003; accepted 23 February 2004) Abstract – A study of the decollement´ zones in the Moffat Shale Group in the Ordovician Northern Belt of the Southern Uplands of Scotland reveals a progressive sequence of deformation and increased channelization of fluid flow. The study concentrates on exposures of imbricated Moffat Shale on the western coast of the Rhins of Galloway. Initial deformation occurred in partially lithified sediments and involved stratal disruption and shearing of the shales. Deformation then became more localized in narrower fault zones characterized by polyphase hydrothermal fluid flow/veining events. -
Mercian 11 B Hunter.Indd
The Cressbrook Dale Lava and Litton Tuff, between Longstone and Hucklow Edges, Derbyshire John Hunter and Richard Shaw Abstract: With only a small exposure near the head of its eponymous dale, the Cressbrook Dale Lava is the least exposed of the major lava flows interbedded within the Carboniferous platform- carbonate succession of the Derbyshire Peak District. It underlies a large area of the limestone plateau between Longstone Edge and the Eyam and Hucklow edges. The recent closure of all of the quarries and underground mines in this area provided a stimulus to locate and compile the existing subsurface information relating to the lava-field and, supplemented by airborne geophysical survey results, to use these data to interpret the buried volcanic landscape. The same sub-surface data-set is used to interpret the spatial distribution of the overlying Litton Tuff. Within the regional north-south crustal extension that survey indicate that the outcrops of igneous rocks in affected central and northern Britain on the north side the White Peak are only part of a much larger volcanic of the Wales-Brabant High during the early part of the field, most of which is concealed at depth beneath Carboniferous, a province of subsiding platforms, tilt- Millstone Grit and Coal Measures farther east. Because blocks and half-grabens developed beneath a shallow no large volcano structures have been discovered so continental sea. Intra-plate magmatism accompanied far, geological literature describes the lavas in the the lithospheric thinning, with basic igneous rocks White Peak as probably originating from four separate erupting at different times from a number of small, local centres, each being active in a different area at different volcanic centres scattered across a region extending times (Smith et al., 2005). -
Ductile Deformation - Concepts of Finite Strain
327 Ductile deformation - Concepts of finite strain Deformation includes any process that results in a change in shape, size or location of a body. A solid body subjected to external forces tends to move or change its displacement. These displacements can involve four distinct component patterns: - 1) A body is forced to change its position; it undergoes translation. - 2) A body is forced to change its orientation; it undergoes rotation. - 3) A body is forced to change size; it undergoes dilation. - 4) A body is forced to change shape; it undergoes distortion. These movement components are often described in terms of slip or flow. The distinction is scale- dependent, slip describing movement on a discrete plane, whereas flow is a penetrative movement that involves the whole of the rock. The four basic movements may be combined. - During rigid body deformation, rocks are translated and/or rotated but the original size and shape are preserved. - If instead of moving, the body absorbs some or all the forces, it becomes stressed. The forces then cause particle displacement within the body so that the body changes its shape and/or size; it becomes deformed. Deformation describes the complete transformation from the initial to the final geometry and location of a body. Deformation produces discontinuities in brittle rocks. In ductile rocks, deformation is macroscopically continuous, distributed within the mass of the rock. Instead, brittle deformation essentially involves relative movements between undeformed (but displaced) blocks. Finite strain jpb, 2019 328 Strain describes the non-rigid body deformation, i.e. the amount of movement caused by stresses between parts of a body. -
Shear Zone-Related Folds
Journal of Structural Geology 27 (2005) 1229–1251 www.elsevier.com/locate/jsg Shear zone-related folds Jordi Carreras, Elena Druguet*, Albert Griera Departament de Geologia, Universitat Auto`noma de Barcelona, 08193 Bellaterra, Spain Received 18 April 2003; received in revised form 27 February 2004; accepted 14 June 2004 Available online 30 November 2004 Abstract Folds in ductile shear zones are common structures that have a variety of origins. These can be pre-existing folds that become modified or folds developed during the shearing event. Among the syn-shearing folds, a second subdivision is based on the relative age of the folded surface, which can be pre-existing or newly formed during the shearing event. In each of the three categories final fold geometry and orientation show complex relationships with the kinematic frame. The final fold geometry depends on the vorticity within the shear zone, the rheology and the initial orientation of the folded surface relative to the kinematic framework. It follows that folds are complex structures, difficult to use as kinematic indicators. However, in shear zones where undeformed wall rocks with pre-shear structures are accessible and where kinematics can be well established, folds can provide a valuable natural means to understand the initiation and evolution of structures under non-coaxial regimes. We point to the need of discriminating among different plausible categories, based on the nature of the folded surface and on the inherent structural features of each category. q 2004 Elsevier Ltd. All rights reserved. Keywords: Fold; Shear zone; Geometry; Kinematics; Cap de Creus 1. Introduction final geometry, symmetry and orientation of a shear-related fold are influenced by many variables other than the shear Folds are common structures in many ductile shear sense.