DOCSLIB.ORG

Cleavage in Some Sedimentary Rocks of the Central Valley and Ridge Province, Maryland

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Cleavage in Some Sedimentary Rocks of the Central Valley and Ridge Province, Maryland Cleavage in Some Sedimentary Rocks of the Central Valley and Ridge Province, Maryland P. A. GEISER Department of Geology, University of Connecticut, Storrs, Connecticut 06268 ABSTRACT Limited field evidence suggests that the preferred orientation shown by burrow cross sections may be controlled by paleocurrent The Cacapon Mountain anticline of the folded Appalachian directions, making the burrows a possible current indicator. Fi- Mountains contains rocks ranging in age from Early Silurian to nally, it is suggested that the fabric imposed by the burrowing or- Early Devonian. The Middle Silurian Bloomsburg Formation ap- ganisms may have localized and controlled the development of the proximates a thin, viscous plate embedded in a less viscous Sp cleavage. Key words: structural geology, finite strain, Silurian medium. The presence of scolithuslike burrows, useful as strain ichnology. markers, makes the Bloomsburg Formation an excellent unit for studying the folding of a sedimentary plate. INTRODUCTION Examination of the microscopic fabric of rock containing a so- This paper analyzes the deformation of some unmetamorphosed called "fracture cleavage" reveals the presence of discontinuous, sedimentary rocks in the folded Appalachian Mountains. Although platy zones containing tectonically oriented quartz and mica frag- numerous strain studies have been made in metamorphic terranes, ments. It is deduced that the shape and orientation of the quartz strain analysis has only infrequently been applied to sedimentary fragments is largely due to differential solution; however, there is rocks that have not undergone regional penetrative deformation some evidence of mechanical rotation of the fragments. As the (Nickelsen, 1966; Breddin, 1956; Plessman, 1966). "fracture cleavage" does not fit the classical definition (being lo- The Bloomsburg Formation in the Cacapon Mountain anticline cally penetrative), it has been designated Sp cleavage for the pur- is a thin (15-m) plate of siliceous siltstone, embedded in a thick se- poses of this paper. quence of incompetent sedimentary rocks. This is physically Finite strain analysis shows that the cleavage postdates analogous to a thin, viscous elastic plate embedded in a less viscous lithification, that it formed perpendicular to bedding and parallel to medium. The Bloomsburg Formation also contains natural strain the plane of the finite strain ellipsoid containing X! and X2, and that markers in the form of small vertical burrows, making it an excel- it is a plane of flattening. The Sp cleavage is interpreted as a lent unit to use in a deformation study. phenomenon marking a transition point in the material behavior of The Hancock region of the Cacapon Mountain anticline (Stose the rock. The transition point was reached after the rock under- and Swartz, 1912, p. 129-131; Swartz, 1923) is located im- went a maximum two-dimensional irreversible strain of e = 0.06. mediately west of Hancock, Maryland (Fig. 1). The anticline lies in This small strain is in contrast to the values of e = 0.30 that have the eastern half of the Valley and Ridge province of the central Ap- been suggested for slaty cleavage. During progressive deformation, palachians and west of the "tectonite" front (Fellows, 1943). the Sp cleavage became structurally passive, permitting it to be used Geologic mapping of the region was done by Stose and Swartz as a strain marker in the determination of strain about fold profiles (1912), and Swartz (1923, p. 152) did detailed stratigraphy. (ac surface). Rocks ranging in age from earliest Silurian to Early Devonian are Geological Society of America Bulletin, v. 85, p. 1399-1412, 19 figs., September 1974 1399 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/85/9/1399/3428958/i0016-7606-85-9-1399.pdf by guest on 29 September 2021 1400 P. A. GEISER Study Samples containing burrows were collected at 17 localities (Fig. Area P*• 2). Where a fold is well exposed, three samples were collected from KWJH anco c k the same bed — a sample from each limb and one from the crest of the fold. At all other localities only one sample was collected. Each sample was cut in three perpendicular directions. The ini- tial cut was perpendicular to the cleavage and approximately paral- lel to bedding (a in Fig. 3). The second cut was perpendicular to W. Va. both bedding and cleavags (b in Fig. 3), and the third cut was paral- lel to cleavage and perpendicular to bedding (c in Fig. 3). DESCRIPTION OF CLEAVAGE IN THE BLOOMSBURG FORMATION The Bloomsburg and lower Wills Creek Formations show a con- sistent cleavage as a conspicuous plane of parting, roughly perpen- dicular to the bedding (Fig. 4). This cleavage, frequently as promi- Figure 1. Location of study area. nent as bedding, has been mentioned only briefly in the literature on the central folded Appalachians. exposed in the anticline. The lower units consist of shale and Gair (1949, p. 30) described it as "appearing to be fracture fine-grained sandstone. The rocks become increasingly calcareous cleavage." Stevens (1959, p. 25—30) referred to "radial joints nor- upward, and the highest units are limestone. A generalized strati- mal to bedding," attributed to early tensional stresses. Cloos graphic column is given in Table 1. (1951, p. 156) described the structure simply as "cleavage normal The structures exposed in the western Maryland railroad cuts at to the bedding and fanning through a large angle." Roundtop and Woodmont have been described by Gair (1949), Both the fanning nature of the cleavage and its occasional sig- Cloos (1951), and Stevens (1959), but there has been no systematic moidal form have been described by Stevens (1959) and Cloos study of strain or use of strain markers. Because the rocks are in the i'1951). Cloos suggested that the cleavage formed early and possi- early stages of deformation, they retain an almost complete strain bly prior to folding. Gair also implied an early origin for the cleav- history. age, finding that the "fracture cleavage" in the Wills Creek induced Finite strain was measured in 20 samples from 17 different no preferred crystallographic orientation. The lack of preferred localities (Fig. 2). X-ray photographs were made of 15 samples to orientation suggested to Gair that the cleavage may have formed reveal internal structure. prior to consolidation. Field Methods. Mapping was done on parts of the two W2' A second type of cleavage found in the Bloomsburg Formation is quadrangles (U.S. Geological Survey, 1951a, 1951b), enlarged to a restricted to the shaly unirs and is characterized by a small angle, scale of 1:6,156. A total of 837 stations were made over the 32.7 between 5° and 45°, made with bedding (B-3 in Fig. 4b). This 2 km mapped, with three to four measurements made per station. In cleavage has been designated Sa. The so-called "fracture cleavage," an effort to utilize as much of the generally poor exposures as pos- approximately perpendicular to bedding, is designated Sp. The two sible, traverses were made close to one another with some lines cleavages never occur in the same bed. only 164 m apart. TABLE 1. GENERALIZE: STRATIGRAPHIC SECTION Sp CLEAVAGE AT HANCCCK, MARYLAND* Macroscopic Description Age Formation Thickness Llthology Or) The Sp cleavage is a set of prominent subparallel irregular sur- faces (Figs. 4a, b), which are usually 1 to 2 cm apart. Examination Oriskany Group 65.5 Massive orthoquartzite; thin, dis- continuous cherty layers at base of the bedding surfaces shows a faint lineation parallel to the Helderberg Formation 52.4 Thin- to massive-bedded limestone cleavage-bedding intersection designated Lx. with occasional shale interbeds or scattered chert layers One of the most consistent characteristics of the cleavage is its angle with bedding. The angles between cleavage and bedding Keyser Limestone 95.} Massive, nodular limestone at base; poles from 130 stations were measured on a stereographic net, and grades upward to thin-bedded limestone with considerable shale the sets were plotted on ?. frequency diagram (Fig. 5). Half the Tonoloway Limestone 132.0 Thin- to medium-bedded laminated angles fall between 82° and 90°; the remainder are scattered over IC limestone with platy appearance the intervals between 58° and 82°. Wills Creek Shale 147.0 Limestone interbedded with calcar- eous shale, sandstone,and mudstone The Sp cleavage ends abruptly at the base of the Bloomsburg Bloomsburg Formation 14.7 Massive red siltstone with a few Formation and gradually disappears upward as the siltstone be- yellow and red shale and sandstone interbeds comes progressively more calcareous and less burrowed. The close correlation between burrowing and Sp cleavage is visi- McKenzie Formation 75.3 Dark calcareous shale and thin argillaceous limestone ble at a number of exposures in a fine-grained sandstone member of Rochester Shale 9.£5 Dark calcareous shale the lower Bloomsburg Formation. The cleavage, well developed in Keefer Sandstone 8.1 Fine- to medium-grain quartz sand- adjacent beds, is completely lacking in the unburrowed sandstone. stone, thin- to medium-bedded Figure 4 shows this relation clearly; S cleavage in burrowed silt- Dark shale with scattered interbeds p of thin- to medium-bedded fine stone ends at the edge of a i>ed (B-3 in Fig. 4b) consisting of inter- Rose Hill Formation 196.5 sandstone bedded shales and sandstone lenses. Thin- to thick-bedded orthoquartzite Tuscarora Formation 124.5 with scattered interbeds of thin Microscopic Description shale Although cleavage is visible in all hand specimens, its develop- * After Swartz (1923Ì. ment varies considerably on the microscopic scale. The framework Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/85/9/1399/3428958/i0016-7606-85-9-1399.pdf by guest on 29 September 2021 CLEAVAGE IN SOME SEDIMENTARY ROCKS OF THE CENTRAL VALLEY AND RIDGE PROVINCE, MARYLAND 1401 of the Bloomsburg siltstone consists of more than 95 percent quartz 42) and Ramsay (1967, p.
Load more

Recommended publications
  • 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.
    [Show full text]
  • 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.
    [Show full text]
  • Collision Orogeny
    Downloaded from http://sp.lyellcollection.org/ by guest on October 6, 2021 PROCESSES OF COLLISION OROGENY Downloaded from http://sp.lyellcollection.org/ by guest on October 6, 2021 Downloaded from http://sp.lyellcollection.org/ by guest on October 6, 2021 Shortening of continental lithosphere: the neotectonics of Eastern Anatolia a young collision zone J.F. Dewey, M.R. Hempton, W.S.F. Kidd, F. Saroglu & A.M.C. ~eng6r SUMMARY: We use the tectonics of Eastern Anatolia to exemplify many of the different aspects of collision tectonics, namely the formation of plateaux, thrust belts, foreland flexures, widespread foreland/hinterland deformation zones and orogenic collapse/distension zones. Eastern Anatolia is a 2 km high plateau bounded to the S by the southward-verging Bitlis Thrust Zone and to the N by the Pontide/Minor Caucasus Zone. It has developed as the surface expression of a zone of progressively thickening crust beginning about 12 Ma in the medial Miocene and has resulted from the squeezing and shortening of Eastern Anatolia between the Arabian and European Plates following the Serravallian demise of the last oceanic or quasi- oceanic tract between Arabia and Eurasia. Thickening of the crust to about 52 km has been accompanied by major strike-slip faulting on the rightqateral N Anatolian Transform Fault (NATF) and the left-lateral E Anatolian Transform Fault (EATF) which approximately bound an Anatolian Wedge that is being driven westwards to override the oceanic lithosphere of the Mediterranean along subduction zones from Cephalonia to Crete, and Rhodes to Cyprus. This neotectonic regime began about 12 Ma in Late Serravallian times with uplift from wide- spread littoral/neritic marine conditions to open seasonal wooded savanna with coiluvial, fluvial and limnic environments, and the deposition of the thick Tortonian Kythrean Flysch in the Eastern Mediterranean.
    [Show full text]
  • Mylonite Zones in the Crystalline Basement Rocks of Sixmile Creek and Yankee Jim Canyon Park County Montana
    University of Montana ScholarWorks at University of Montana Graduate Student Theses, Dissertations, & Professional Papers Graduate School 1982 Mylonite zones in the crystalline basement rocks of Sixmile Creek and Yankee Jim Canyon Park County Montana Robert Robert Burnham The University of Montana Follow this and additional works at: https://scholarworks.umt.edu/etd Let us know how access to this document benefits ou.y Recommended Citation Burnham, Robert Robert, "Mylonite zones in the crystalline basement rocks of Sixmile Creek and Yankee Jim Canyon Park County Montana" (1982). Graduate Student Theses, Dissertations, & Professional Papers. 4677. https://scholarworks.umt.edu/etd/4677 This Thesis is brought to you for free and open access by the Graduate School at ScholarWorks at University of Montana. It has been accepted for inclusion in Graduate Student Theses, Dissertations, & Professional Papers by an authorized administrator of ScholarWorks at University of Montana. For more information, please contact [email protected]. COPYRIGHT ACT OF 1976 This is an unpublished manuscript in which copyright sub ­ s is t s . Any further reprinting of its contents must be approved BY THE AUTHOR. Mansfield Library U niversity of Montana Date: 19 8 2 MYLONITE ZONES IN THE CRYSTALLINE BASEMENT ROCKS OF SIXMILE CREEK AND YANKEE JIM CANYON, PARK COUNTY, MONTANA by Robert Burnham B.A., Dartmouth, 1980 Presented in partial fulfillment of the requirements for the degree of Master of Science UNIVERSITY OF MONTANA 1982 Approved by: UMI Number: EP40141 All rights reserved INFORMATION TO ALL USERS The quality of this reproduction is dependent upon the quality of the copy submitted. In the unlikely event that the author did not send a complete manuscript and there are missing pages, these will be noted.
    [Show full text]
  • Metamorphic Fabrics
    11/30/2015 Geol341 J. Toro Topics • Fabrics • Foliation, cleavage, lineation Metamorphic Rocks and – Cleavage and Folds –Geometry Cleavage Development – Strain significance • Origin of Cleavage – Pressure solution – Passive rotation – Recrystallization • Shear zones Many diagrams are from Earth Structure, van der Pluijm and Marshak, 2004 2013 Geothermal Gradient and Metamorphism Naming of Metamorphic Rocks Slatey cleavage Gneiss Segregation of mafic and felsic components Where does it come from? 1 11/30/2015 Looks like bedding, but is it? Metamorphic layering Brooks Range, AK Quartz-mica schist Isoclinal Fold Transposition of Layering Fabric “Arrangement of component features in a rock” van der Pluijm & Marshak •Includes: •Texture •Composition •Microstructure •Preferred Orientation Horizontal fabric => Vertical fabric 2 11/30/2015 Quartz-mica schist Fabric Elements •Bedding (S0) •Compositional layering •Crystallographic orientation •Fold Hinges •Cleavage planes (S1) •Mineral elongation lineation Passchier and Trouw (1996) Metamorphic Fabrics Metamorphic Fabrics • Foliation : Cleavage, Schistosity • Foliation • Lineation: Mineral Lineation, Intersection Lineation – Cleavage – Schistosity • Lineation Random fabric S-tectonite L-tectonite L/S-tectonite Foliation Lineation S-Tectonites L-Tectonites Schists Columbia Pluton, VA Lineated Gneiss USGS photo U. Western Ontario photo 3 11/30/2015 L-S Tectonites 3D Strain - Flinn diagram No strain along 3rd dimension Cigars S =S >S S1/S2 1 2 3 S1>S2=S3 Lineated and foliated gneiss, Himalayas Prolate
    [Show full text]
  • Fracture Cleavage'' in the Duluth Complex, Northeastern Minnesota
    Downloaded from gsabulletin.gsapubs.org on August 9, 2013 Geological Society of America Bulletin ''Fracture cleavage'' in the Duluth Complex, northeastern Minnesota M. E. FOSTER and P. J. HUDLESTON Geological Society of America Bulletin 1986;97, no. 1;85-96 doi: 10.1130/0016-7606(1986)97<85:FCITDC>2.0.CO;2 Email alerting services click www.gsapubs.org/cgi/alerts to receive free e-mail alerts when new articles cite this article Subscribe click www.gsapubs.org/subscriptions/ to subscribe to Geological Society of America Bulletin Permission request click http://www.geosociety.org/pubs/copyrt.htm#gsa to contact GSA Copyright not claimed on content prepared wholly by U.S. government employees within scope of their employment. Individual scientists are hereby granted permission, without fees or further requests to GSA, to use a single figure, a single table, and/or a brief paragraph of text in subsequent works and to make unlimited copies of items in GSA's journals for noncommercial use in classrooms to further education and science. This file may not be posted to any Web site, but authors may post the abstracts only of their articles on their own or their organization's Web site providing the posting includes a reference to the article's full citation. GSA provides this and other forums for the presentation of diverse opinions and positions by scientists worldwide, regardless of their race, citizenship, gender, religion, or political viewpoint. Opinions presented in this publication do not reflect official positions of the Society. Notes Geological Society of America Downloaded from gsabulletin.gsapubs.org on August 9, 2013 "Fracture cleavage" in the Duluth Complex, northeastern Minnesota M.
    [Show full text]
  • 2 Review of Stress, Linear Strain and Elastic Stress- Strain Relations
    2 Review of Stress, Linear Strain and Elastic Stress- Strain Relations 2.1 Introduction In metal forming and machining processes, the work piece is subjected to external forces in order to achieve a certain desired shape. Under the action of these forces, the work piece undergoes displacements and deformation and develops internal forces. A measure of deformation is defined as strain. The intensity of internal forces is called as stress. The displacements, strains and stresses in a deformable body are interlinked. Additionally, they all depend on the geometry and material of the work piece, external forces and supports. Therefore, to estimate the external forces required for achieving the desired shape, one needs to determine the displacements, strains and stresses in the work piece. This involves solving the following set of governing equations : (i) strain-displacement relations, (ii) stress- strain relations and (iii) equations of motion. In this chapter, we develop the governing equations for the case of small deformation of linearly elastic materials. While developing these equations, we disregard the molecular structure of the material and assume the body to be a continuum. This enables us to define the displacements, strains and stresses at every point of the body. We begin our discussion on governing equations with the concept of stress at a point. Then, we carry out the analysis of stress at a point to develop the ideas of stress invariants, principal stresses, maximum shear stress, octahedral stresses and the hydrostatic and deviatoric parts of stress. These ideas will be used in the next chapter to develop the theory of plasticity.
    [Show full text]
  • 4. Deep-Tow Observations at the East Pacific Rise, 8°45N, and Some Interpretations
    4. DEEP-TOW OBSERVATIONS AT THE EAST PACIFIC RISE, 8°45N, AND SOME INTERPRETATIONS Peter Lonsdale and F. N. Spiess, University of California, San Diego, Marine Physical Laboratory, Scripps Institution of Oceanography, La Jolla, California ABSTRACT A near-bottom survey of a 24-km length of the East Pacific Rise (EPR) crest near the Leg 54 drill sites has established that the axial ridge is a 12- to 15-km-wide lava plateau, bounded by steep 300-meter-high slopes that in places are large outward-facing fault scarps. The plateau is bisected asymmetrically by a 1- to 2-km-wide crestal rift zone, with summit grabens, pillow walls, and axial peaks, which is the locus of dike injection and fissure eruption. About 900 sets of bottom photos of this rift zone and adjacent parts of the plateau show that the upper oceanic crust is composed of several dif- ferent types of pillow and sheet lava. Sheet lava is more abundant at this rise crest than on slow-spreading ridges or on some other fast- spreading rises. Beyond 2 km from the axis, most of the plateau has a patchy veneer of sediment, and its surface is increasingly broken by extensional faults and fissures. At the plateau's margins, secondary volcanism builds subcircular peaks and partly buries the fault scarps formed on the plateau and at its boundaries. Another deep-tow survey of a patch of young abyssal hills 20 to 30 km east of the spreading axis mapped a highly lineated terrain of inactive horsts and grabens. They were created by extension on inward- and outward- facing normal faults, in a zone 12 to 20 km from the axis.
    [Show full text]
  • Fracture Characterization Mapping for Regional Geologic Studies: the Hydrostructural Domain Approach, Ayer Quadrangle, Massachusetts
    Fracture Characterization Mapping for Regional Geologic Studies: The Hydrostructural Domain Approach, Ayer Quadrangle, Massachusetts Stephen B. Mabee And Joseph P. Kopera Office of the Massachusetts State Geologist Geosciences Department University of Massachusetts 611 North Pleasant Street Amherst, MA 01003 Abstract While traditional bedrock geologic maps contain valuable information, they commonly lack data on brittle fracture characteristics and distributions. The increased need for better understanding of groundwater flow behavior in bedrock aquifers has made this data critical. The concept of hydrostructural domains is used to redefine bedrock mapping units based on an assemblage of lithologic and fracture characteristics thought to be important controls on groundwater flow and recharge. These maps are constructed from detailed field observations and measurements of 2000-3000 fractures from 60-70 stations across a 7.5' quadrangle. Hydrostructural domains are displayed on the map as traditional lithologic units would be, with detailed descriptions and photos of the fracture systems contained in each hydrostructural “unit”. In the Ayer quadrangle, such domains closely correspond with bedrock lithology and ductile structural history. Steeply dipping metasedimentary rocks of the Merrimack Belt have pervasive, closely spaced, throughgoing fractures developed parallel to foliation, and therefore may provide excellent potential for vertical recharge and foliation-parallel flow. Where these rocks are intensely cut by a strong subhorizontal cleavage, a parallel fracture set dominates providing an opportunity for lateral flow. Massive granites generally have a well-developed, widely-spaced orthogonal network of fracture zones which may provide excellent local recharge. High-grade gneisses of the Nashoba formation have poorly developed fracture sets except near regional shear zones, where foliation parallel fractures and cross-joints may provide good vertical recharge and provide a strong northeast trending flow anisotropy.
    [Show full text]
  • Paleostress and Remote Sensing Analysis of Brittle Fractures from the Eastern Margin of the Dead Sea Transform, Jordan”
    Masaryk University Faculty of Sciences Department of Geological Sciences “Paleostress and Remote Sensing Analysis of Brittle Fractures from the Eastern Margin of the Dead Sea Transform, Jordan” ―Literature Thesis in Requirement for Doctor of Philosophy in Geology Degree Program‖ Prepared by: M.Sc. Omar Mohammad Radaideh Supervisors: Assoc. Prof. RNDr. Rostislav Melichar Brno, Czech Republic 2013 OUTLINES CONTENTS ……………………………………………………………...……………………… II LIST OF FIGURES………………………………………………………………………………. III LIST OF TABLE…………………………………………………………….…………………… III CONTENTS PAGE 1. INTODUCTION 1 2. GEOLOGICAL AND TECTONIC SETTING 2 2.1 General Geological Overview 5 2.2 Major Tectonic Elements 3. SIGNIFICANCE AND OBJECTIVES OF THE STUDY 7 4. METHODOLOGY 8 4.1 Paleostress 8 4.2 Remote Sensing 13 4.2.1. Linear stretching 16 4.2.2. Principal Components Analysis 16 4.2.3. Band ratios 17 4.2.4. Edge Enhancement 17 4.2.5. Intensity/Hue/Saturation (HIS) transformations 18 5. PREVIOUS STUDIES 19 5.1. Paleostress Analysis in Jordan 20 5.2. Paleostress in the Sinai-Israel Sub-Plate 22 5.3. Paleostress in the East Mediterranean 25 5.4. Summary of Paleostress Results 28 REFERENCES 28 II LIST OF FIGUERS Figure Page Figure 1: Location map of the study area…………………………………………………………… 1 Figure 2: Simplified geological map of the southwestern Jordan……………………………...…… 3 Figure 3: The Main tectonic features of the Dead Sea Transform………………………………….. 6 Figure 4: Generalized structure map of Jordan……………………………………………………... 7 Figure 5: Schematic flowchart illustrating the methods and steps that will be used in this study….. 8 Figure 6: Stress ratio and stress ellipsoid…………………………………………………………… 9 Figure 7: The relationship between stress and ideal faults………………………………………….
    [Show full text]
  • PLANE DIP and STRIKE, LINEATION PLUNGE and TREND, STRUCTURAL MEASURMENT CONVENTIONS, the BRUNTON COMPASS, FIELD BOOK, and NJGS FMS
    PLANE DIP and STRIKE, LINEATION PLUNGE and TREND, STRUCTURAL MEASURMENT CONVENTIONS, THE BRUNTON COMPASS, FIELD BOOK, and NJGS FMS The word azimuth stems from an Arabic word meaning "direction“, and means an angular measurement in a spherical coordinate system. In structural geology, we primarily deal with land navigation and directional readings on two-dimensional maps of the Earth surface, and azimuth commonly refers to incremental measures in a circular (0- 360 °) and horizontal reference frame relative to land surface. Sources: Lisle, R. J., 2004, Geological Structures and Maps, A Practical Guide, Third edition http://www.geo.utexas.edu/courses/420k/PDF_files/Brunton_Compass_09.pdf http://en.wikipedia.org/wiki/Azimuth http://en.wikipedia.org/wiki/Brunton_compass FLASH DRIVE/Rider/PDFs/Holcombe_conv_and_meas.pdf http://www.state.nj.us/dep/njgs/geodata/fmsdoc/fmsuser.htm Brunton Pocket Transit Rider Structural Geology 310 2012 GCHERMAN 1 PlanePlane DipDip andand LinearLinear PlungePlunge horizontal dddooo Dip = dddooo Bedding and other geological layers and planes that are not horizontal are said to dip. The dip is the slope of a geological surface. There are two aspects to the dip of a plane: (a) the direction of dip , which is the compass direction towards which the plane slopes; and (b) the angle of dip , which is the angle that the plane makes with a horizontal plane (Fig. 2.3). The direction of dip can be visualized as the direction in which water would flow if poured onto the plane. The angle of dip is an angle between 0 ° (for horizontal planes) and 90 ° (for vertical planes). To record the dip of a plane all that is needed are two numbers; the angle of dip followed by the direction (or azimuth) of dip, e.g.
    [Show full text]
  • Stylolites: a Review
    Stylolites: a review Toussaint R.1,2,3*, Aharonov E.4, Koehn, D.5, Gratier, J.-P.6, Ebner, M.7, Baud, P.1, Rolland, A.1, and Renard, F.6,8 1Institut de Physique du Globe de Strasbourg, CNRS, University of Strasbourg, 5 rue Descartes, F- 67084 Strasbourg Cedex, France. Phone : +33 673142994. email : [email protected] 2 International Associate Laboratory D-FFRACT, Deformation, Flow and Fracture of Disordered Materials, France-Norway. 3SFF PoreLab, The Njord Centre, Department of Physics, University of Oslo, Norway. 4Institute of Earth Sciences, The Hebrew University, Jerusalem, 91904, Israel 5School of Geographical and Earth Sciences, University of Glasgow, UK 6University Grenoble Alpes, ISTerre, Univ. Savoie Mont Blanc, CNRS, IRD, IFSTTAR, 38000 Grenoble, France 7OMV Exploration & Production GmbH Trabrennstrasse 6-8, 1020 Vienna, Austria 8 The Njord Centre,PGP, Department of Geosciences, University of Oslo, Norway *corresponding author Highlights: . Stylolite formation depends on rock composition and structure, stress and fluids. Stylolite geometry, fractal and self-affine properties, network structure, are investigated. The experiments and physics-based numerical models for their formation are reviewed. Stylolites can be used as markers of strain, paleostress orientation and magnitude. Stylolites impact transport properties, as function of maturity and flow direction. Abstract Stylolites are ubiquitous geo-patterns observed in rocks in the upper crust, from geological reservoirs in sedimentary rocks to deformation zones, in folds, faults, and shear zones. These rough surfaces play a major role in the dissolution of rocks around stressed contacts, the transport of dissolved material and the precipitation in surrounding pores. Consequently, they 1 play an active role in the evolution of rock microstructures and rheological properties in the Earth’s crust.
    [Show full text]