Plate Tectonics – Practice Questions and Answers Revised August 2007
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Slab Pull? Density of Plate Slab
The plate tectonic story www.earthscienceeducation.com Geography Workshop GA Conference 2021 Duncan Hawley in association with the Earth Science Education Unit and EarthLearningIdea www.earthlearningidea.com Image: Free download https://www.kissclipart.com/visual-tectonic-plates-clipart-crust-earth-plate-t-nnw9dx/ The plate tectonic story www.earthscienceeducation.com Aims of this session The workshop and its activities aims to: • provide an integrated overview of the concepts involved in teaching the processes of plate tectonics at KS3, KS4 and A level • survey of some of the recent evidence and key ideas in understanding how plate tectonics works • offer improved explanations for the distribution and characteristics of volcanoes, earthquakes, and some surface landforms • suggest approaches to teaching the abstract concepts of plate tectonics • help teachers decide if and how they should adjust what they presently teach to reflect the current understanding about the way plate tectonics operates • help teachers develop students’ critical sense of ‘the plate tectonic story’ encountered in textbooks, on diagrams, on the news, via the internet and in other media. The plate tectonic story www.earthscienceeducation.com Where on Earth are earthquakes and volcanoes? - geobattleships www.earthlearningidea.com/PDF/79_Geobattleships.pdf Battleship grid for Geobattleships © Dave Turner Galunggung eruption by USGS, public domain ‘North All Trucks’ © USGS The plate tectonic story www.earthscienceeducation.com Where on Earth are earthquakes and volcanoes? -
Slab-Pull and Slab-Push Earthquakes in the Mexican, Chilean and Peruvian Subduction Zones A
Physics of the Earth and Planetary Interiors 132 (2002) 157–175 Slab-pull and slab-push earthquakes in the Mexican, Chilean and Peruvian subduction zones A. Lemoine a,∗, R. Madariaga a, J. Campos b a Laboratoire de Géologie, Ecole Normale Supérieure, 24 Rue Lhomond, 75231 Paris Cedex 05, France b Departamento de Geof´ısica, Universidad de Chile, Santiago, Chile Abstract We studied intermediate depth earthquakes in the Chile, Peru and Mexican subduction zones, paying special attention to slab-push (down-dip compression) and slab-pull (down-dip extension) mechanisms. Although, slab-push events are relatively rare in comparison with slab-pull earthquakes, quite a few have occurred recently. In Peru, a couple slab-push events occurred in 1991 and one slab-pull together with several slab-push events occurred in 1970 near Chimbote. In Mexico, several slab-push and slab-pull events occurred near Zihuatanejo below the fault zone of the 1985 Michoacan event. In central Chile, a large M = 7.1 slab-push event occurred in October 1997 that followed a series of four shallow Mw > 6 thrust earthquakes on the plate interface. We used teleseismic body waveform inversion of a number of Mw > 5.9 slab-push and slab-pull earthquakes in order to obtain accurate mechanisms, depths and source time functions. We used a master event method in order to get relative locations. We discussed the occurrence of the relatively rare slab-push events in the three subduction zones. Were they due to the geometry of the subduction that produces flexure inside the downgoing slab, or were they produced by stress transfer during the earthquake cycle? Stress transfer can not explain the occurence of several compressional and extensional intraplate intermediate depth earthquakes in central Chile, central Mexico and central Peru. -
ASSESSMENT of the TSUNAMIGENIC POTENTIAL ALONG the NORTHERN CARIBBEAN MARGIN Case Study: Earthquake and Tsunamis of 12 January 2010 in Haiti
ISSN 87556839 SCIENCE OF TSUNAMI HAZARDS Journal of Tsunami Society International Volume 29 Number 3 2010 ASSESSMENT OF THE TSUNAMIGENIC POTENTIAL ALONG THE NORTHERN CARIBBEAN MARGIN Case Study: Earthquake and Tsunamis of 12 January 2010 in Haiti. George Pararas-Carayannis Tsunami Society International, Honolulu, Hawaii 96815, USA [email protected] ABSTRACT The potential tsunami risk for Hispaniola, as well as for the other Greater Antilles Islands is assessed by reviewing the complex geotectonic processes and regimes along the Northern Caribbean margin, including the convergent, compressional and collisional tectonic activity of subduction, transition, shearing, lateral movements, accretion and crustal deformation caused by the eastward movement of the Caribbean plate in relation to the North American plate. These complex tectonic interactions have created a broad, diffuse tectonic boundary that has resulted in an extensive, internal deformational sliver slab - the Gonâve microplate – as well as further segmentation into two other microplates with similarly diffused boundary characteristics where tsunamigenic earthquakes have and will again occur. The Gonâve microplate is the most prominent along the Northern Caribbean margin and extends from the Cayman Spreading Center to Mona Pass, between Puerto Rico and the island of Hispaniola, where the 1918 destructive tsunami was generated. The northern boundary of this sliver microplate is defined by the Oriente strike-slip fault south of Cuba, which appears to be an extension of the fault system traversing the northern part of Hispaniola, while the southern boundary is defined by another major strike-slip fault zone where the Haiti earthquake of 12 January 2010 occurred. Potentially tsunamigenic regions along the Northern Caribbean margin are located not only along the boundaries of the Gonâve microplate’s dominant western transform zone but particularly within the eastern tectonic regimes of the margin where subduction is dominant - particularly along the Puerto Rico trench. -
Advanced Geodynamics: Fourier Transform Methods
Advanced Geodynamics: Fourier Transform Methods David T. Sandwell January 13, 2021 To Susan, Katie, Melissa, Nick, and Cassie Eddie Would Go Preprint for publication by Cambridge University Press, October 16, 2020 Contents 1 Observations Related to Plate Tectonics 7 1.1 Global Maps . .7 1.2 Exercises . .9 2 Fourier Transform Methods in Geophysics 20 2.1 Introduction . 20 2.2 Definitions of Fourier Transforms . 21 2.3 Fourier Sine and Cosine Transforms . 22 2.4 Examples of Fourier Transforms . 23 2.5 Properties of Fourier transforms . 26 2.6 Solving a Linear PDE Using Fourier Methods and the Cauchy Residue Theorem . 29 2.7 Fourier Series . 32 2.8 Exercises . 33 3 Plate Kinematics 36 3.1 Plate Motions on a Flat Earth . 36 3.2 Triple Junction . 37 3.3 Plate Motions on a Sphere . 41 3.4 Velocity Azimuth . 44 3.5 Recipe for Computing Velocity Magnitude . 45 3.6 Triple Junctions on a Sphere . 45 3.7 Hot Spots and Absolute Plate Motions . 46 3.8 Exercises . 46 4 Marine Magnetic Anomalies 48 4.1 Introduction . 48 4.2 Crustal Magnetization at a Spreading Ridge . 48 4.3 Uniformly Magnetized Block . 52 4.4 Anomalies in the Earth’s Magnetic Field . 52 4.5 Magnetic Anomalies Due to Seafloor Spreading . 53 4.6 Discussion . 58 4.7 Exercises . 59 ii CONTENTS iii 5 Cooling of the Oceanic Lithosphere 61 5.1 Introduction . 61 5.2 Temperature versus Depth and Age . 65 5.3 Heat Flow versus Age . 66 5.4 Thermal Subsidence . 68 5.5 The Plate Cooling Model . -
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. -
On the Dynamics of the Juan De Fuca Plate
Earth and Planetary Science Letters 189 (2001) 115^131 www.elsevier.com/locate/epsl On the dynamics of the Juan de Fuca plate Rob Govers *, Paul Th. Meijer Faculty of Earth Sciences, Utrecht University, P.O. Box 80.021, 3508 TA Utrecht, The Netherlands Received 11 October 2000; received in revised form 17 April 2001; accepted 27 April 2001 Abstract The Juan de Fuca plate is currently fragmenting along the Nootka fault zone in the north, while the Gorda region in the south shows no evidence of fragmentation. This difference is surprising, as both the northern and southern regions are young relative to the central Juan de Fuca plate. We develop stress models for the Juan de Fuca plate to understand this pattern of breakup. Another objective of our study follows from our hypothesis that small plates are partially driven by larger neighbor plates. The transform push force has been proposed to be such a dynamic interaction between the small Juan de Fuca plate and the Pacific plate. We aim to establish the relative importance of transform push for Juan de Fuca dynamics. Balancing torques from plate tectonic forces like slab pull, ridge push and various resistive forces, we first derive two groups of force models: models which require transform push across the Mendocino Transform fault and models which do not. Intraplate stress orientations computed on the basis of the force models are all close to identical. Orientations of predicted stresses are in agreement with observations. Stress magnitudes are sensitive to the force model we use, but as we have no stress magnitude observations we have no means of discriminating between force models. -
The Way the Earth Works: Plate Tectonics
CHAPTER 2 The Way the Earth Works: Plate Tectonics Marshak_ch02_034-069hr.indd 34 9/18/12 2:58 PM Chapter Objectives By the end of this chapter you should know . > Wegener's evidence for continental drift. > how study of paleomagnetism proves that continents move. > how sea-floor spreading works, and how geologists can prove that it takes place. > that the Earth’s lithosphere is divided into about 20 plates that move relative to one another. > the three kinds of plate boundaries and the basis for recognizing them. > how fast plates move, and how we can measure the rate of movement. We are like a judge confronted by a defendant who declines to answer, and we must determine the truth from the circumstantial evidence. —Alfred Wegener (German scientist, 1880–1930; on the challenge of studying the Earth) 2.1 Introduction In September 1930, fifteen explorers led by a German meteo- rologist, Alfred Wegener, set out across the endless snowfields of Greenland to resupply two weather observers stranded at a remote camp. The observers had been planning to spend the long polar night recording wind speeds and temperatures on Greenland’s polar plateau. At the time, Wegener was well known, not only to researchers studying climate but also to geologists. Some fifteen years earlier, he had published a small book, The Origin of the Con- tinents and Oceans, in which he had dared to challenge geologists’ long-held assumption that the continents had remained fixed in position through all of Earth history. Wegener thought, instead, that the continents once fit together like pieces of a giant jigsaw puzzle, to make one vast supercontinent. -
MAGNITUDE of DRIVING FORCES of PLATE MOTION Since the Plate
J. Phys. Earth, 33, 369-389, 1985 THE MAGNITUDE OF DRIVING FORCES OF PLATE MOTION Shoji SEKIGUCHI Disaster Prevention Research Institute, Kyoto University, Uji, Kyoto, Japan (Received February 22, 1985; Revised July 25, 1985) The absolute magnitudes of a variety of driving forces that could contribute to the plate motion are evaluated, on the condition that all lithospheric plates are in dynamic equilibrium. The method adopted here is to solve the equations of torque balance of these forces for all plates, after having estimated the magnitudes of the ridge push and slab pull forces from known quantities. The former has been estimated from the age of ocean floors, the depth and thickness of oceanic plates and hence lateral density variations, and the latter from the density con- trast between the downgoing slab and the surrounding mantle, and the thickness and length of the slab. The results from the present calculations show that the magnitude of the slab pull forces is about five times larger than that of the ridge push forces, while the North American and South American plates, which have short and shallow slabs but long oceanic ridges, appear to be driven by the ridge push force. The magnitude of the slab pull force exerted on the Pacific plate exceeds to 40 % of the total slab pull forces, and that of the ridge push force working on the Pacific plate is the largest among the ridge push forces exerted on the plates. The high cor- relation that exists between the mantle drag force and the sum of the slab pull and ridge push forces makes it difficult to evaluate the absolute net driving forces. -
An Evidence-Based Approach to Teaching Plate Tectonics in High School
An evidence-based approach to teaching plate tectonics in high school COLIN PRICE ABSTRACT 5. relating the extreme age and stability of a large part of the Australian continent to its plate tectonic This article proposes an evidence-based and engaging history. approach to teaching the mechanisms driving the movement of tectonic plates that should lead high The problem with this list is the fourth elaboration, school students towards the prevalent theories because the idea that convection currents in the used in peer-reviewed science journals and taught mantle drive the movement of tectonic plates is a in universities. The methods presented replace the myth. This convection is presented as whole mantle inaccurate and outdated focus on mantle convection as or whole asthenosphere cells with hot material rising the driving mechanism for plate motion. Students frst under the Earth’s divergent plate boundaries and examine the relationship between the percentages of cooler material sinking at the convergent boundaries plate boundary types of the 14 largest plates with their with the lithosphere dragged along by the horizontal GPS-determined plate speeds to then evaluate the fow of the asthenosphere (Figure 1). This was the three possible driving mechanisms: mantle convection, preferred explanation for plate motion until the ridge push and slab pull. A classroom experiment early 1990s but it does not stand up to a frequent measuring the densities of igneous and metamorphic deduction made by Year 9 students: how can there be rocks associated with subduction zones then provides large-scale mantle convection if hotspots (like Hawaii) a plausible explanation for slab pull as the dominant don’t move? Most science teachers quickly cover driving mechanism. -
The Relation Between Mantle Dynamics and Plate Tectonics
The History and Dynamics of Global Plate Motions, GEOPHYSICAL MONOGRAPH 121, M. Richards, R. Gordon and R. van der Hilst, eds., American Geophysical Union, pp5–46, 2000 The Relation Between Mantle Dynamics and Plate Tectonics: A Primer David Bercovici , Yanick Ricard Laboratoire des Sciences de la Terre, Ecole Normale Superieure´ de Lyon, France Mark A. Richards Department of Geology and Geophysics, University of California, Berkeley Abstract. We present an overview of the relation between mantle dynam- ics and plate tectonics, adopting the perspective that the plates are the surface manifestation, i.e., the top thermal boundary layer, of mantle convection. We review how simple convection pertains to plate formation, regarding the aspect ratio of convection cells; the forces that drive convection; and how internal heating and temperature-dependent viscosity affect convection. We examine how well basic convection explains plate tectonics, arguing that basic plate forces, slab pull and ridge push, are convective forces; that sea-floor struc- ture is characteristic of thermal boundary layers; that slab-like downwellings are common in simple convective flow; and that slab and plume fluxes agree with models of internally heated convection. Temperature-dependent vis- cosity, or an internal resistive boundary (e.g., a viscosity jump and/or phase transition at 660km depth) can also lead to large, plate sized convection cells. Finally, we survey the aspects of plate tectonics that are poorly explained by simple convection theory, and the progress being made in accounting for them. We examine non-convective plate forces; dynamic topography; the deviations of seafloor structure from that of a thermal boundary layer; and abrupt plate- motion changes. -
Presentation on Pacific Plate and Associated Boundaries
PACIFIC PLATE AND ASSOCIATED BOUNDARIES The Pacific Plate • Pacific Plate is the largest plate and an oceanic plate. • It shares its boundaries with numerous plates namely; North American Plate.(Convergent and transform fault) Philippine Plate.(Convergent) Juan de Fuca Plate.(Convergent) Indo – Australian Plate.(Convergent, Transform Fault) Cocos Plate.(Divergent) Nazca Plate.(Divergent) Antarctic Plate.(Divergent,Transform Fault) Types of Plate Boundaries • Convergent Boundary: Subduction zones where two plates converges. Eg; Aleutian Islands(Alaska) • Divergent Boundary: Spreading centres where two plates move away from each other. Eg; East Pacific Rise (MOR, Pacific Ocean). • Transform Faults: Boundary where two plates slide past each other. For Eg. ; San Andreas Fault. BOUNDARY WITH ANTARCTIC PLATE DIVERGENT BOUNDARY • Pacific – Antarctic Ridge TRANSFORM FAULT • Louisville Seamount Chain Pacific – Antarctic Ridge Pacific – Antarctic Ridge(PAR) is located on the seafloor of the South Pacific Ocean. It is driven by the interaction of a mid oceanic ridge and deep mantle plumes located in the eastern portion of East Pacific Ridge. Louisville Seamount Chain It is the longest line of seamount chain in the Pacific Ocean of about 4,300 km, formed along the transform boundary in the western side between Pacific plate and Antarctic plate. It was formed from the Pacific Plate sliding over a long – lived centre of upwelling magma called the Louisville hotspot. BOUNDARY WITH PHILIPPINE PLATE CONVERGENT BOUNDARY • Izu – Ogasawara Trench • Mariana Trench Izu – Ogasawara Trench It is an oceanic trench in the western Pacific Ocean. It stretches from Japan to northern most section of Mariana Trench. Here, the Pacific Plate is being subducted beneath the Philippine Sea Plate. -
'Sounding the Pacific Ocean; an Echo Sounder Traverse of the Eastern Pacific'
Earthlearningidea - https://www.earthlearningidea.com/ Sounding the Pacific Ocean An echo sounder traverse of the eastern Pacific Ask them to describe out loud the main changes in depth to their partner in the class, and to discuss if they found any of these surprising, and if so, why. (Answers will vary, but the rapid descent into the Peru/Chile Trench may be a surprise: also the monotonously flat section and the sudden rise to the seamount). Ask them to label the following on their graphs: Continental shelf – depth less than 150m Continental slope – depths from 150m to 2000m Peru/Chile Trench – depth of 8000m The harbour at Callao, Lima, Peru in 2005. Abyssal plain – very level sea bed at around A research ship sets out from the coast of Peru, 5000m depth near Lima, and travels due west for 3600km. As Seamount – isolated underwater peak rising to the ship moves, its echo sounder is continuously 2000m or less below sea level recording the depth of the ocean floor below sea East Pacific Rise –an underwater mountain level. Some of the echo sounder readings are range at around 2000m depth shown in the Table. The Table shows the distance Rift valley of the East Pacific Rise – around from Lima in kilometres and the time taken for the 3500m depth. echo sounder’s ‘ping’ to travel from the transmitter Ask what they would expect to happen to the in the ship’s hull and back up again to the water depth as the ship sails a few hundred receiver. We know that the speed of sound in sea kilometres further west.