Example Orthographic Solutions to Apparent Dip, True Dip, 3-Point
Total Page:16
File Type:pdf, Size:1020Kb
Load more
Recommended publications
-
Strike and Dip Refer to the Orientation Or Attitude of a Geologic Feature. The
Name__________________________________ 89.325 – Geology for Engineers Faults, Folds, Outcrop Patterns and Geologic Maps I. Properties of Earth Materials When rocks are subjected to differential stress the resulting build-up in strain can cause deformation. Depending on the material properties the result can either be elastic deformation which can ultimately lead to the breaking of the rock material (faults) or ductile deformation which can lead to the development of folds. In this exercise we will look at the various types of deformation and how geologists use geologic maps to understand this deformation. II. Strike and Dip Strike and dip refer to the orientation or attitude of a geologic feature. The strike line of a bed, fault, or other planar feature, is a line representing the intersection of that feature with a horizontal plane. On a geologic map, this is represented with a short straight line segment oriented parallel to the strike line. Strike (or strike angle) can be given as either a quadrant compass bearing of the strike line (N25°E for example) or in terms of east or west of true north or south, a single three digit number representing the azimuth, where the lower number is usually given (where the example of N25°E would simply be 025), or the azimuth number followed by the degree sign (example of N25°E would be 025°). The dip gives the steepest angle of descent of a tilted bed or feature relative to a horizontal plane, and is given by the number (0°-90°) as well as a letter (N, S, E, W) with rough direction in which the bed is dipping. -
Field Geology
FIELD GEOLOGY GUIDEBOOK AND NOTES ILLINOIS STATE UNIVERSITY 2018 Version 2 Table of Contents Syllabus 5 Schedule 8 Hazard Recognition Mitigation 9 Geologic Field Notes 17 Reconnaissance Notes 17 Measuring Stratigraphic Column Notes 18 Geologic Mapping Notes 19 Geologic Maps and Mapping 22 Variables affecting the appearance of a geologic map 23 Techniques to test the quality and accuracy of your map 23 Common map errors 24 Official USGS map colors 24 Rule of V’s 25 Geologic Cross Sections 26 Basic principles of cross section construction 26 Apparent dips: correct use of strike and dip data in cross sections 27 Common cross section errors 27 Steps in making a topographic profile for a geologic cross section 28 Constructing geologic cross sections using down-plunge projection 29 Phanerozoic Stratigraphy of North America 33 Tectonic History of the U.S. Cordillera 38 Regional Cross-sections through Wyoming 41 Wyoming Stratigraphic Nomenclature Chart 42 Rock Sequence in the Bighorn Basin 43 Rock Sequence in the Powder River Basin 44 Black Hills Precambrian Geology 45 Project Descriptions 47 Regional Stratigraphy 47 Amsden Creek Big Game Winter Range 49 Steerhead Ranch 50 Alkali 53 South Fork 55 Mickelson 57 Moonshine 60 Appendix 1: Essential Analysis Tools and Techniques for Field Geology 62 Field description of rocks 62 Measuring stratigraphic sections 69 Calculating layer thicknesses 76 Alignment diagram for calculating apparent dip 77 Calculating strike and dip of a surface from contacts on a map 78 Calculating outcrop patterns from field -
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. -
FM 5-410 Chapter 2
FM 5-410 CHAPTER 2 Structural Geology Structural geology describes the form, pat- secondary structural features. These secon- tern, origin, and internal structure of rock dary features include folds, faults, joints, and and soil masses. Tectonics, a closely related schistosity. These features can be identified field, deals with structural features on a and m appeal in the field through site inves- larger regional, continental, or global scale. tigation and from remote imagery. Figure 2-1, page 2-2, shows the major plates of the earth’s crust. These plates continually Section I. Structural Features undergo movement as shown by the arrows. in Sedimentary Rocks Figure 2-2, page 2-3, is a more detailed repre- sentation of plate tectonic theory. Molten material rises to the earth’s surface at BEDDING PLANES midoceanic ridges, forcing the oceanic plates Structural features are most readily recog- to diverge. These plates, in turn, collide with nized in the sedimentary rocks. They are adjacent plates, which may or may not be of normally deposited in more or less regular similar density. If the two colliding plates are horizontal layers that accumulate on top of of approximately equal density, the plates each other in an orderly sequence. Individual will crumple, forming mountain range along deposits within the sequence are separated the convergent zone. If, on the other hand, by planar contact surfaces called bedding one of the plates is more dense than the other, planes (see Figure 1-7, page 1-9). Bedding it will be subducted, or forced below, the planes are of great importance to military en- lighter plate, creating an oceanic trench along gineers. -
Structural Geology
2 STRUCTURAL GEOLOGY Conventional Map A map is a proportionate representation of an area/structure. The study of maps is known as cartography and the experts are known as cartographers. The maps were first prepared by people of Sumerian civilization by using clay lens. The characteristic elements of a map are scale (ratio of map distance to field distance and can be represented in three ways—statement method, e.g., 1 cm = 0.5 km, representative fraction method, e.g., 1:50,000 and graphical method in the form of a figure), direction, symbol and colour. On the basis of scale, maps are of two types: large-scale map (map gives more information pertaining to a smaller area, e.g., village map: 1:3956) and small: scale map (map gives less information pertaining to a larger area, e.g., world atlas: 1:100 km). Topographic Maps / Toposheet A toposheet is a map representing topography of an area. It is prepared by the Survey of India, Dehradun. Here, a three-dimensional feature is represented on a two-dimensional map and the information is mainly represented by contours. The contours/isohypses are lines connecting points of same elevation with respect to mean sea level (msl). The index contours are the contours representing 100’s/multiples of 100’s drawn with thick lines. The contour interval is usually 20 m. The contours never intersect each other and are not parallel. The characteristic elements of a toposheet are scale, colour, symbol and direction. The various layers which can be prepared from a toposheet are structural elements like fault and lineaments, cropping pattern, land use/land cover, groundwater abstruction structures, drainage density, drainage divide, elongation ratio, circularity ratio, drainage frequency, natural vegetation, rock types, landform units, infrastructural facilities, drainage and waterbodies, drainage number, drainage pattern, drainage length, relief/slope, stream order, sinuosity index and infiltration number. -
Chromium Chemistry in Natural Waters, Iceland Deformation Mechanisms in Martian Shergottites
1414 Goldschmidt2013 Conference Abstracts Chromium chemistry in natural Deformation mechanisms in Martian waters, Iceland Shergottites HANNA KAASALAINEN1*, ANDRI STEFÁNSSON1, KACZMAREK M.-A.*12, GRANGE M.1, REDDY S.M.1, INGVI GUNNARSSON2 AND STEFÁN ARNÓRSSON1 AND NEMCHIN A.1 1Institute of Earth Sciences, University of Iceland, Sturlugata 1Department of Applied Geology, The Institute for Geoscience 7, 101 Reykjavik, Iceland, Research, Curtin University of Technology, GPO Box (*correspondence: [email protected]) U1987, Perth, WA 6845, Australia 2Present address: Reykjavik Energy, Bæjarhalsi 1, 110 2Now at University of Lausanne, Institute of Earth Sciences, Reykajvik, Iceland UNIL Mouline, Géopolis, CH-1016 Lausanne, Switzerland Chemistry of Cr and Fe was studied in non-thermal and (*correspondence: [email protected]) geothermal waters in Iceland. Chromium (Cr) is typically present at low concentrations (<1 µg/l) in natural waters, but Nakhla and Zagami are both clinopyroxene-rich basaltic elevated concentrations have been observed in waters with shergottite, with some Fe-rich olivine. The microstructure, the low pH values, e.g. acid mine drainage, and in association preferred orientation of pyroxene using Electron Backscatter with industrial activities. Chromium occurs in two oxidation Diffraction (EBSD) method and the gochemistry are combined states, Cr(III) and (VI), these being characterized by different to study subsamples of both Zagami and Nakhla to decipher (bio)chemical behaviour and solubility. As Cr(VI) is known to deformation processes that have occurred on Mars. be toxic but Cr(III) an essential micronutrient, it is important Nakhla displays a granular texture, essentially composed to determine the two oxidations states. Iron (Fe) is known to of augite, fayalite, plagioclase and magnetite. -
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. -
Faulted Joints: Kinematics, Displacement±Length Scaling Relations and Criteria for Their Identi®Cation
Journal of Structural Geology 23 (2001) 315±327 www.elsevier.nl/locate/jstrugeo Faulted joints: kinematics, displacement±length scaling relations and criteria for their identi®cation Scott J. Wilkinsa,*, Michael R. Grossa, Michael Wackera, Yehuda Eyalb, Terry Engelderc aDepartment of Geology, Florida International University, Miami, FL 33199, USA bDepartment of Geology, Ben Gurion University, Beer Sheva 84105, Israel cDepartment of Geosciences, The Pennsylvania State University, University Park, PA 16802, USA Received 6 December 1999; accepted 6 June 2000 Abstract Structural geometries and kinematics based on two sets of joints, pinnate joints and fault striations, reveal that some mesoscale faults at Split Mountain, Utah, originated as joints. Unlike many other types of faults, displacements (D) across faulted joints do not scale with lengths (L) and therefore do not adhere to published fault scaling laws. Rather, fault size corresponds initially to original joint length, which in turn is controlled by bed thickness for bed-con®ned joints. Although faulted joints will grow in length with increasing slip, the total change in length is negligible compared to the original length, leading to an independence of D from L during early stages of joint reactivation. Therefore, attempts to predict fault length, gouge thickness, or hydrologic properties based solely upon D±L scaling laws could yield misleading results for faulted joints. Pinnate joints, distinguishable from wing cracks, developed within the dilational quadrants along faulted joints and help to constrain the kinematics of joint reactivation. q 2001 Elsevier Science Ltd. All rights reserved. 1. Introduction impact of these ªfaulted jointsº on displacement±length scaling relations and fault-slip kinematics. -
Using THEMIS Images of Mars Graben in a Structural Geology Course
Using THEMIS Images of Mars Graben in a Structural Geology Course Barbara Tewksbury Hamilton College [email protected] What do students do in Why go to Mars for examples of this activity? normal fault systems? What prior knowledge do students need? • Before class, students complete a homework assignment that • On Earth, even young, active normal faults are modified rapidly by familiarizes them with accessing and downloading Mars erosion and deposition, obscuring the surface expression of features. THEMIS images and in which they download images of normal • This activity is written assuming that students know the general faults in the Ceraunius Fossae of northern Tharsis. terminology for normal fault systems (graben, horst, relay ramp, • On Mars, by contrast, one can find relatively pristine normal fault • In class, I start with a short discussion about how THEMIS images hangingwall block, heave, throw, dip, etc.). The exercise also is features in which very little modification has occurred. are obtained, why the images are in strips, what resolution written assuming that students can figure out how to use trig to means, and so on. solve for fault heave and throw. • Mars normal faults offer an ideal opportunity for students to study the • Students then examine their Mars images and identify normal features of real normal fault systems in map view, rather than simply in fault features. • The activity would be very easy to modify, however, so that it stylized map-view diagrams in textbooks, and to gain experience in • Students determine the range of graben widths and then calculate could be done by students who have very little background in recognizing features in a pristine setting that students can transfer to throw for one fault using shadow width to calculate graben structural geology or who would struggle trying to figure out the studying normal fault systems on Earth. -
Structural Geology of Parautochthonous and Allochthonous Terranes of the Penokean Orogeny in Upper Michigan Comparisons with Northern Appalachian Tectonics
Structural Geology of Parautochthonous and Allochthonous Terranes of the Penokean Orogeny in Upper Michigan Comparisons with Northern Appalachian Tectonics U.S. GEOLOGICAL SURVEY BULLETIN 1904-Q AVAILABILITY OF BOOKS AND MAPS OF THE U.S. GEOLOGICAL SURVEY Instructions on ordering publications of the U.S. Geological Survey, along with the last offerings, are given in the current-year issues of the monthly catalog "New Publications of the U.S. Geological Survey." Prices of available U.S. Geological Survey publications released prior to the current year are listed in the most recent annual "Price and Availability List." Publications that are listed in various U.S. Geological Survey catalogs (see back inside cover) but not listed in the most recent annual "Price and Availability List" are no longer available. Prices of reports released to the open files are given in the listing "U.S. Geological Survey Open-File Reports," updated monthly, which is for sale in microfiche from the U.S. Geological Survey, Book and Open-File Report Sales, Box 25286, Building 810, Denver Federal Center, Denver, CO 80225 Order U.S. Geological Survey publications by mail or over the counter from the offices given below. BY MAIL OVER THE COUNTER Books Books Professional Papers, Bulletins, Water-Supply Papers, Tech Books of the U.S. Geological Survey are available over the niques of Water-Resources Investigations, Circulars, publications counter at the following U.S. Geological Survey offices, all of of general interest (such as leaflets, pamphlets, booklets), single which are authorized agents of the Superintendent of Documents. copies of periodicals (Earthquakes & Volcanoes, Preliminary De termination of Epicenters), and some miscellaneous reports, includ ANCHORAGE, Alaska-Rm. -
Evidence for Controlled Deformation During Laramide Orogeny
Geologic structure of the northern margin of the Chihuahua trough 43 BOLETÍN DE LA SOCIEDAD GEOLÓGICA MEXICANA D GEOL DA Ó VOLUMEN 60, NÚM. 1, 2008, P. 43-69 E G I I C C O A S 1904 M 2004 . C EX . ICANA A C i e n A ñ o s Geologic structure of the northern margin of the Chihuahua trough: Evidence for controlled deformation during Laramide Orogeny Dana Carciumaru1,*, Roberto Ortega2 1 Orbis Consultores en Geología y Geofísica, Mexico, D.F, Mexico. 2 Centro de Investigación Científi ca y de Educación Superior de Ensenada (CICESE) Unidad La Paz, Mirafl ores 334, Fracc.Bella Vista, La Paz, BCS, 23050, Mexico. *[email protected] Abstract In this article we studied the northern part of the Laramide foreland of the Chihuahua Trough. The purpose of this work is twofold; fi rst we studied whether the deformation involves or not the basement along crustal faults (thin- or thick- skinned deformation), and second, we studied the nature of the principal shortening directions in the Chihuahua Trough. In this region, style of deformation changes from motion on moderate to low angle thrust and reverse faults within the interior of the basin to basement involved reverse faulting on the adjacent platform. Shortening directions estimated from the geometry of folds and faults and inversion of fault slip data indicate that both basement involved structures and faults within the basin record a similar Laramide deformation style. Map scale relationships indicate that motion on high angle basement involved thrusts post dates low angle thrusting. This is consistent with the two sets of faults forming during a single progressive deformation with in - sequence - thrusting migrating out of the basin onto the platform. -
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.