{"id":284,"date":"2014-12-04T19:51:58","date_gmt":"2014-12-04T19:51:58","guid":{"rendered":"https:\/\/courses.candelalearning.com\/env131fmusu14\/?post_type=chapter&#038;p=284"},"modified":"2017-10-11T17:27:37","modified_gmt":"2017-10-11T17:27:37","slug":"tectonic-stress-and-geologic-structures-2","status":"publish","type":"chapter","link":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/chapter\/tectonic-stress-and-geologic-structures-2\/","title":{"raw":"Tectonic Stress and Geologic Structures","rendered":"Tectonic Stress and Geologic Structures"},"content":{"raw":"<div id=\"wsite-content\" class=\"wsite-elements wsite-not-footer\">\r\n<h2 class=\"wsite-content-title\" style=\"text-align: left\">Causes and Types of Tectonic Stress<\/h2>\r\n<span style=\"width: auto;float: right;max-width: 100%;;clear: right;margin-top: 5px\"><a href=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/1392170009.jpg\"><img class=\"galleryImageBorder wsite-image\" style=\"border-width: 0;max-width: 100%;margin: 5px 0px 10px 10px\" src=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/1392170009.jpg\" alt=\"Picture\" \/><\/a><\/span>\r\n<div class=\"paragraph\" style=\"text-align: left\">Enormous slabs of lithosphere move unevenly over the planet\u2019s spherical surface, resulting in earthquakes. This chapter deals with two types of geological activity that occur because of plate tectonics: mountain building and earthquakes. First, we will consider what can happen to rocks when they are exposed to stress.\u00a0<strong><a href=\"http:\/\/earthquake.usgs.gov\/learn\/glossary\/?term=stress\" target=\"_blank\">Stress<\/a><\/strong> is the force applied to an object. In geosciences, stress is the force per unit area that is placed on a rock. Four types of stresses act on materials.\r\n<ul>\r\n\t<li>A deeply buried rock is pushed down by the weight of all the material above it. Since the rock cannot move, it cannot deform called <strong>confining stress<\/strong>.<\/li>\r\n\t<li><strong><a href=\"http:\/\/earthquake.usgs.gov\/learn\/glossary\/?term=compressional%20stress\" target=\"_blank\">Compression<\/a><\/strong> squeezes rocks together, causing rocks to fold or fracture. Compression is the most common stress at convergent plate boundaries.<\/li>\r\n<\/ul>\r\n<ul>\r\n\t<li>Rocks that are pulled apart are under <strong>tension<\/strong>. Rocks under tension lengthen or break apart. Tension is the major type of stress at divergent plate boundaries.<\/li>\r\n\t<li>When forces are parallel but moving in opposite directions, the stress is called shear. <strong>Shear<\/strong> stress is the most common stress at transform plate boundaries.<\/li>\r\n<\/ul>\r\nWhen stress causes a material to change shape, it has undergone strain or <strong><a href=\"http:\/\/earthquake.usgs.gov\/learn\/glossary\/?term=deformation\" target=\"_blank\">deformation<\/a><\/strong>. Deformed rocks are common in geologically active areas. A rock\u2019s response to stress depends on the rock type, the surrounding temperature, and pressure conditions the rock is under, the length of time the rock is under stress, and the type of stress. The rocks then have three possible responses to increasing stress: elastic deformation, plastic deformation, or fracturing. <strong>Elastic deformation<\/strong> occurs when the rock returns to its original shape when the stress is removed. When rocks under stress do not return to its original shape when the stress is removed, it is called <strong>plastic deformation<\/strong>. Finally, when a rock under stress breaks, it\u2019s called a <strong>fracture<\/strong>.\r\n\r\nUnder what conditions do you think a rock is more likely to fracture? Is it more likely to break deep within Earth\u2019s crust or at the surface? What if the stress applied is sharp rather than gradual? At the Earth's surface, rocks usually break quite quickly, but deeper in the crust, where temperatures and pressures are higher, rocks are more likely to deform plastically. Sudden stress, such as a hit with a hammer, is more likely to make a rock break. Stress applied over time often leads to plastic def\r\n\r\n<\/div>\r\n\r\n<hr style=\"width: 100%;clear: both\" \/>\r\n\r\n<div>\r\n<div style=\"height: 20px;overflow: hidden;width: 100%\"><\/div>\r\n\r\n<hr class=\"styled-hr\" style=\"width: 100%\" \/>\r\n\r\n<div style=\"height: 20px;overflow: hidden;width: 100%\"><\/div>\r\n<\/div>\r\n<h2 class=\"wsite-content-title\" style=\"text-align: left\">Geologic Structures<\/h2>\r\n<div class=\"paragraph\" style=\"text-align: left\">Sedimentary rocks are important for deciphering the geologic history of a region because they follow certain rules. First, sedimentary rocks are formed with the oldest layers on the bottom and the youngest on top. Second, sediments are deposited horizontally, so sedimentary rock layers are originally horizontal, as are some volcanic rocks, such as ash falls. Finally, sedimentary rock layers that are not horizontal are deformed in some manner. Often times looking like they are tiling into the earth.\r\n\r\nYou can trace the deformation a rock has experienced by seeing how it differs from its original horizontal, oldest-on-bottom position. This deformation produces geologic structures such as folds, joints, and faults that are caused by stresses.<\/div>\r\n<span style=\"width: auto;float: right;max-width: 100%;;clear: right;margin-top: 20px\"><a href=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/2651574.png\"><img class=\"galleryImageBorder wsite-image\" style=\"border-width: 1px;padding: 3px;max-width: 100%;margin: 5px 0px 10px 10px\" src=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/2651574.png\" alt=\"Picture\" \/><\/a><\/span>\r\n<div class=\"paragraph\" style=\"text-align: left\"><span style=\"line-height: 1.5\"><span style=\"color: #c2743b\">FOLDS<\/span><\/span>\r\nRocks deforming plastically under compressive stresses crumple into folds. They do not return to their original shape. If the rocks experience more stress, they may undergo more folding or even fracture. There are three major types of rock folding: monoclines, synclines, and anticlines. A <strong>monocline<\/strong> is a simple bend in the rock layers so that they are no longer horizontal. <strong>Anticlines<\/strong> are folded rocks that arch upward and dip away from the center of the fold. The oldest rocks are at the center of an anticline and the youngest are draped over them. When rocks arch upward to form a circular structure, that structure is called an <strong>adome<\/strong>. A <strong>syncline<\/strong> is a fold that bends downward, causing the youngest rocks are to be at the center and the oldest are on the outside. When rocks bend downward in a circular structure, that structure is called <strong>abasin<\/strong>. If the rocks are exposed at the surface, where are the oldest rocks located?<\/div>\r\n\r\n<hr style=\"width: 100%;clear: both\" \/>\r\n\r\n<div>\r\n<div class=\"wsite-multicol\">\r\n<div class=\"wsite-multicol-table-wrap\" style=\"margin: 0 -15px\">\r\n<table class=\"wsite-multicol-table\">\r\n<tbody class=\"wsite-multicol-tbody\">\r\n<tr class=\"wsite-multicol-tr\">\r\n<td class=\"wsite-multicol-col\" style=\"width: 50%;padding: 0 15px\">\r\n<div>\r\n<div class=\"wsite-image wsite-image-border-thin \" style=\"padding-top: 10px;padding-bottom: 10px;margin-left: 0;margin-right: 0;text-align: center\"><a href=\"http:\/\/en.wikipedia.org\/wiki\/File:Monocline01.svg\" target=\"_blank\">\r\n<\/a><a href=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/731083977.png\"><img style=\"width: auto;max-width: 100%\" src=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/731083977.png\" alt=\"Picture\" \/><\/a>\r\n<div style=\"font-size: 90%\">Monocline diagram<\/div>\r\n<\/div>\r\n<\/div><\/td>\r\n<td class=\"wsite-multicol-col\" style=\"width: 50%;padding: 0 15px\">\r\n<div>\r\n<div class=\"wsite-image wsite-image-border-thin \" style=\"padding-top: 10px;padding-bottom: 10px;margin-left: 0;margin-right: 0;text-align: center\"><a href=\"http:\/\/en.wikipedia.org\/wiki\/File:Antecline_(PSF).png\" target=\"_blank\">\r\n<\/a><a href=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/659151644.png\"><img style=\"width: 100%;max-width: 609px\" src=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/sm_659151644.jpg\" alt=\"Picture\" \/><\/a>\r\n<div style=\"font-size: 90%\"><\/div>\r\n<\/div>\r\n<\/div><\/td>\r\n<\/tr>\r\n<\/tbody>\r\n<\/table>\r\n<\/div>\r\n<\/div>\r\n<\/div>\r\n<span style=\"width: auto;float: left;max-width: 100%;;clear: left;margin-top: 9px\"><a href=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/278459335.jpg\"><img class=\"galleryImageBorder wsite-image\" style=\"border-width: 1px;padding: 3px;max-width: 100%;margin: 5px 10px 10px 0px\" src=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/278459335.jpg\" alt=\"Picture\" \/><\/a><\/span>\r\n<div class=\"paragraph\" style=\"text-align: left\"><span style=\"color: #c2743b\">FAULTS<\/span>\r\nA rock under enough stress will eventually fracture. If there is no movement on either side of a fracture, the fracture is called a <strong>joint<\/strong>. But if the blocks of rock on one or both sides of a fracture move, the fracture is called a fault. Sudden motions along faults cause rocks to break and move suddenly, releasing the stored up stress energy to create an earthquake.\r\n\r\nA <strong>slip<\/strong> is the distance rocks move along a fault and can be up or down the fault plane. Slip is relative, because there is usually no way to know whether both sides moved or only one. Faults lie at an angle to the horizontal surface of the Earth. That angle is called the fault\u2019s <strong>dip<\/strong>. The dip defines which of two basic types a fault is. If the fault\u2019s dip is inclined relative to the horizontal, the fault is a dip-slip fault. There are two types of <strong><a href=\"http:\/\/earthquake.usgs.gov\/learn\/glossary\/?term=dip%20slip\" target=\"_blank\">dip-slip faults<\/a><\/strong>. In <strong><a title=\"\" href=\"http:\/\/earthquake.usgs.gov\/learn\/animations\/animation.php?flash_title=Normal+Fault&amp;flash_file=normalfault&amp;flash_width=220&amp;flash_height=320\" target=\"_blank\">normal faults<\/a><\/strong>, the hanging wall drops down relative to the footwall.\u00a0Normal faults can be huge and are often times responsible for uplifting mountain ranges in regions experiencing tensional stress.\r\n\r\nWith <strong>reverse faults<\/strong>, the footwall drops down relative to the hanging wall.\u00a0A type of reverse fault is a\u00a0<a style=\"font-weight: bold\" title=\"\" href=\"http:\/\/earthquake.usgs.gov\/learn\/animations\/animation.php?flash_title=Thrust+Fault&amp;flash_file=thrustfault&amp;flash_width=220&amp;flash_height=320\" target=\"_blank\">thrust fault<\/a>, in\u00a0which the fault plane angle is nearly horizontal. Rocks can slip many miles along thrust faults.\r\n\r\nA <a title=\"\" href=\"http:\/\/earthquake.usgs.gov\/learn\/animations\/animation.php?flash_title=Strike-Slip+Fault&amp;flash_file=strikeslip&amp;flash_width=240&amp;flash_height=310\" target=\"_blank\"><strong>strike-slip fault<\/strong><\/a> is a dip-slip fault in which the dip of the fault plane is vertical and result from shear stresses.\u00a0<span style=\"line-height: 1.5\">California\u2019s San Andreas Fault is the world\u2019s most famous strike-slip fault. It is a right-lateral strike slip fault.\u00a0<\/span>\r\n\r\n<span style=\"color: #c2743b\">STRESS AND MOUNTAIN BUILDING<\/span>\r\nIt is the shear power and strength of two or more converging continental plates smash upwards that create mountain ranges. Stresses from this uplift cause folds, reverse faults, and thrust faults, which allow the crust to rise upwards. Subduction of oceanic lithosphere at convergent plate boundaries also builds mountain ranges.\r\n\r\nWhen\u00a0<a title=\"\" href=\"http:\/\/earthquake.usgs.gov\/learn\/animations\/animation.php?flash_title=Horst+%26amp%3B+Graben&amp;flash_file=horstandgraben&amp;flash_width=380&amp;flash_height=210\" target=\"_blank\">tensional stresses<\/a>\u00a0pull crust apart, it breaks into blocks that slide up and drop down along normal faults. The result is alternating mountains and valleys, known as a basin-and-range.<\/div>\r\n<div class=\"paragraph\" style=\"text-align: left\"><\/div>\r\n<\/div>","rendered":"<div id=\"wsite-content\" class=\"wsite-elements wsite-not-footer\">\n<h2 class=\"wsite-content-title\" style=\"text-align: left\">Causes and Types of Tectonic Stress<\/h2>\n<p><span style=\"width: auto;float: right;max-width: 100%;;clear: right;margin-top: 5px\"><a href=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/1392170009.jpg\"><img decoding=\"async\" class=\"galleryImageBorder wsite-image\" style=\"border-width: 0;max-width: 100%;margin: 5px 0px 10px 10px\" src=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/1392170009.jpg\" alt=\"Picture\" \/><\/a><\/span><\/p>\n<div class=\"paragraph\" style=\"text-align: left\">Enormous slabs of lithosphere move unevenly over the planet\u2019s spherical surface, resulting in earthquakes. This chapter deals with two types of geological activity that occur because of plate tectonics: mountain building and earthquakes. First, we will consider what can happen to rocks when they are exposed to stress.\u00a0<strong><a href=\"http:\/\/earthquake.usgs.gov\/learn\/glossary\/?term=stress\" target=\"_blank\">Stress<\/a><\/strong> is the force applied to an object. In geosciences, stress is the force per unit area that is placed on a rock. Four types of stresses act on materials.<\/p>\n<ul>\n<li>A deeply buried rock is pushed down by the weight of all the material above it. Since the rock cannot move, it cannot deform called <strong>confining stress<\/strong>.<\/li>\n<li><strong><a href=\"http:\/\/earthquake.usgs.gov\/learn\/glossary\/?term=compressional%20stress\" target=\"_blank\">Compression<\/a><\/strong> squeezes rocks together, causing rocks to fold or fracture. Compression is the most common stress at convergent plate boundaries.<\/li>\n<\/ul>\n<ul>\n<li>Rocks that are pulled apart are under <strong>tension<\/strong>. Rocks under tension lengthen or break apart. Tension is the major type of stress at divergent plate boundaries.<\/li>\n<li>When forces are parallel but moving in opposite directions, the stress is called shear. <strong>Shear<\/strong> stress is the most common stress at transform plate boundaries.<\/li>\n<\/ul>\n<p>When stress causes a material to change shape, it has undergone strain or <strong><a href=\"http:\/\/earthquake.usgs.gov\/learn\/glossary\/?term=deformation\" target=\"_blank\">deformation<\/a><\/strong>. Deformed rocks are common in geologically active areas. A rock\u2019s response to stress depends on the rock type, the surrounding temperature, and pressure conditions the rock is under, the length of time the rock is under stress, and the type of stress. The rocks then have three possible responses to increasing stress: elastic deformation, plastic deformation, or fracturing. <strong>Elastic deformation<\/strong> occurs when the rock returns to its original shape when the stress is removed. When rocks under stress do not return to its original shape when the stress is removed, it is called <strong>plastic deformation<\/strong>. Finally, when a rock under stress breaks, it\u2019s called a <strong>fracture<\/strong>.<\/p>\n<p>Under what conditions do you think a rock is more likely to fracture? Is it more likely to break deep within Earth\u2019s crust or at the surface? What if the stress applied is sharp rather than gradual? At the Earth&#8217;s surface, rocks usually break quite quickly, but deeper in the crust, where temperatures and pressures are higher, rocks are more likely to deform plastically. Sudden stress, such as a hit with a hammer, is more likely to make a rock break. Stress applied over time often leads to plastic def<\/p>\n<\/div>\n<hr style=\"width: 100%;clear: both\" \/>\n<div>\n<div style=\"height: 20px;overflow: hidden;width: 100%\"><\/div>\n<hr class=\"styled-hr\" style=\"width: 100%\" \/>\n<div style=\"height: 20px;overflow: hidden;width: 100%\"><\/div>\n<\/div>\n<h2 class=\"wsite-content-title\" style=\"text-align: left\">Geologic Structures<\/h2>\n<div class=\"paragraph\" style=\"text-align: left\">Sedimentary rocks are important for deciphering the geologic history of a region because they follow certain rules. First, sedimentary rocks are formed with the oldest layers on the bottom and the youngest on top. Second, sediments are deposited horizontally, so sedimentary rock layers are originally horizontal, as are some volcanic rocks, such as ash falls. Finally, sedimentary rock layers that are not horizontal are deformed in some manner. Often times looking like they are tiling into the earth.<\/p>\n<p>You can trace the deformation a rock has experienced by seeing how it differs from its original horizontal, oldest-on-bottom position. This deformation produces geologic structures such as folds, joints, and faults that are caused by stresses.<\/p><\/div>\n<p><span style=\"width: auto;float: right;max-width: 100%;;clear: right;margin-top: 20px\"><a href=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/2651574.png\"><img decoding=\"async\" class=\"galleryImageBorder wsite-image\" style=\"border-width: 1px;padding: 3px;max-width: 100%;margin: 5px 0px 10px 10px\" src=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/2651574.png\" alt=\"Picture\" \/><\/a><\/span><\/p>\n<div class=\"paragraph\" style=\"text-align: left\"><span style=\"line-height: 1.5\"><span style=\"color: #c2743b\">FOLDS<\/span><\/span><br \/>\nRocks deforming plastically under compressive stresses crumple into folds. They do not return to their original shape. If the rocks experience more stress, they may undergo more folding or even fracture. There are three major types of rock folding: monoclines, synclines, and anticlines. A <strong>monocline<\/strong> is a simple bend in the rock layers so that they are no longer horizontal. <strong>Anticlines<\/strong> are folded rocks that arch upward and dip away from the center of the fold. The oldest rocks are at the center of an anticline and the youngest are draped over them. When rocks arch upward to form a circular structure, that structure is called an <strong>adome<\/strong>. A <strong>syncline<\/strong> is a fold that bends downward, causing the youngest rocks are to be at the center and the oldest are on the outside. When rocks bend downward in a circular structure, that structure is called <strong>abasin<\/strong>. If the rocks are exposed at the surface, where are the oldest rocks located?<\/div>\n<hr style=\"width: 100%;clear: both\" \/>\n<div>\n<div class=\"wsite-multicol\">\n<div class=\"wsite-multicol-table-wrap\" style=\"margin: 0 -15px\">\n<table class=\"wsite-multicol-table\">\n<tbody class=\"wsite-multicol-tbody\">\n<tr class=\"wsite-multicol-tr\">\n<td class=\"wsite-multicol-col\" style=\"width: 50%;padding: 0 15px\">\n<div>\n<div class=\"wsite-image wsite-image-border-thin\" style=\"padding-top: 10px;padding-bottom: 10px;margin-left: 0;margin-right: 0;text-align: center\"><a href=\"http:\/\/en.wikipedia.org\/wiki\/File:Monocline01.svg\" target=\"_blank\"><br \/>\n<\/a><a href=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/731083977.png\"><img decoding=\"async\" style=\"width: auto;max-width: 100%\" src=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/731083977.png\" alt=\"Picture\" \/><\/a><\/p>\n<div style=\"font-size: 90%\">Monocline diagram<\/div>\n<\/div>\n<\/div>\n<\/td>\n<td class=\"wsite-multicol-col\" style=\"width: 50%;padding: 0 15px\">\n<div>\n<div class=\"wsite-image wsite-image-border-thin\" style=\"padding-top: 10px;padding-bottom: 10px;margin-left: 0;margin-right: 0;text-align: center\"><a href=\"http:\/\/en.wikipedia.org\/wiki\/File:Antecline_(PSF).png\" target=\"_blank\"><br \/>\n<\/a><a href=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/659151644.png\"><img decoding=\"async\" style=\"width: 100%;max-width: 609px\" src=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/sm_659151644.jpg\" alt=\"Picture\" \/><\/a><\/p>\n<div style=\"font-size: 90%\"><\/div>\n<\/div>\n<\/div>\n<\/td>\n<\/tr>\n<\/tbody>\n<\/table>\n<\/div>\n<\/div>\n<\/div>\n<p><span style=\"width: auto;float: left;max-width: 100%;;clear: left;margin-top: 9px\"><a href=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/278459335.jpg\"><img decoding=\"async\" class=\"galleryImageBorder wsite-image\" style=\"border-width: 1px;padding: 3px;max-width: 100%;margin: 5px 10px 10px 0px\" src=\"https:\/\/s3-us-west-2.amazonaws.com\/candimgs\/YtLB5q\/278459335.jpg\" alt=\"Picture\" \/><\/a><\/span><\/p>\n<div class=\"paragraph\" style=\"text-align: left\"><span style=\"color: #c2743b\">FAULTS<\/span><br \/>\nA rock under enough stress will eventually fracture. If there is no movement on either side of a fracture, the fracture is called a <strong>joint<\/strong>. But if the blocks of rock on one or both sides of a fracture move, the fracture is called a fault. Sudden motions along faults cause rocks to break and move suddenly, releasing the stored up stress energy to create an earthquake.<\/p>\n<p>A <strong>slip<\/strong> is the distance rocks move along a fault and can be up or down the fault plane. Slip is relative, because there is usually no way to know whether both sides moved or only one. Faults lie at an angle to the horizontal surface of the Earth. That angle is called the fault\u2019s <strong>dip<\/strong>. The dip defines which of two basic types a fault is. If the fault\u2019s dip is inclined relative to the horizontal, the fault is a dip-slip fault. There are two types of <strong><a href=\"http:\/\/earthquake.usgs.gov\/learn\/glossary\/?term=dip%20slip\" target=\"_blank\">dip-slip faults<\/a><\/strong>. In <strong><a title=\"\" href=\"http:\/\/earthquake.usgs.gov\/learn\/animations\/animation.php?flash_title=Normal+Fault&amp;flash_file=normalfault&amp;flash_width=220&amp;flash_height=320\" target=\"_blank\">normal faults<\/a><\/strong>, the hanging wall drops down relative to the footwall.\u00a0Normal faults can be huge and are often times responsible for uplifting mountain ranges in regions experiencing tensional stress.<\/p>\n<p>With <strong>reverse faults<\/strong>, the footwall drops down relative to the hanging wall.\u00a0A type of reverse fault is a\u00a0<a style=\"font-weight: bold\" title=\"\" href=\"http:\/\/earthquake.usgs.gov\/learn\/animations\/animation.php?flash_title=Thrust+Fault&amp;flash_file=thrustfault&amp;flash_width=220&amp;flash_height=320\" target=\"_blank\">thrust fault<\/a>, in\u00a0which the fault plane angle is nearly horizontal. Rocks can slip many miles along thrust faults.<\/p>\n<p>A <a title=\"\" href=\"http:\/\/earthquake.usgs.gov\/learn\/animations\/animation.php?flash_title=Strike-Slip+Fault&amp;flash_file=strikeslip&amp;flash_width=240&amp;flash_height=310\" target=\"_blank\"><strong>strike-slip fault<\/strong><\/a> is a dip-slip fault in which the dip of the fault plane is vertical and result from shear stresses.\u00a0<span style=\"line-height: 1.5\">California\u2019s San Andreas Fault is the world\u2019s most famous strike-slip fault. It is a right-lateral strike slip fault.\u00a0<\/span><\/p>\n<p><span style=\"color: #c2743b\">STRESS AND MOUNTAIN BUILDING<\/span><br \/>\nIt is the shear power and strength of two or more converging continental plates smash upwards that create mountain ranges. Stresses from this uplift cause folds, reverse faults, and thrust faults, which allow the crust to rise upwards. Subduction of oceanic lithosphere at convergent plate boundaries also builds mountain ranges.<\/p>\n<p>When\u00a0<a title=\"\" href=\"http:\/\/earthquake.usgs.gov\/learn\/animations\/animation.php?flash_title=Horst+%26amp%3B+Graben&amp;flash_file=horstandgraben&amp;flash_width=380&amp;flash_height=210\" target=\"_blank\">tensional stresses<\/a>\u00a0pull crust apart, it breaks into blocks that slide up and drop down along normal faults. The result is alternating mountains and valleys, known as a basin-and-range.<\/div>\n<div class=\"paragraph\" style=\"text-align: left\"><\/div>\n<\/div>\n\n\t\t\t <section class=\"citations-section\" role=\"contentinfo\">\n\t\t\t <h3>Candela Citations<\/h3>\n\t\t\t\t\t <div>\n\t\t\t\t\t\t <div id=\"citation-list-284\">\n\t\t\t\t\t\t\t <div class=\"licensing\"><div class=\"license-attribution-dropdown-subheading\">CC licensed content, Shared previously<\/div><ul class=\"citation-list\"><li>Tectonic Forces. <strong>Provided by<\/strong>: Open Geography Education. <strong>Located at<\/strong>: <a target=\"_blank\" href=\"http:\/\/www.opengeography.org\/ch-5-tectonic-forces.html\">http:\/\/www.opengeography.org\/ch-5-tectonic-forces.html<\/a>. <strong>Project<\/strong>: Dynamic Earth: Introduction to Physical Geography. <strong>License<\/strong>: <em><a target=\"_blank\" rel=\"license\" href=\"https:\/\/creativecommons.org\/licenses\/by-nc\/4.0\/\">CC BY-NC: Attribution-NonCommercial<\/a><\/em><\/li><\/ul><\/div>\n\t\t\t\t\t\t <\/div>\n\t\t\t\t\t <\/div>\n\t\t\t <\/section>","protected":false},"author":5,"menu_order":1,"template":"","meta":{"_candela_citation":"[{\"type\":\"cc\",\"description\":\"Tectonic Forces\",\"author\":\"\",\"organization\":\"Open Geography Education\",\"url\":\"http:\/\/www.opengeography.org\/ch-5-tectonic-forces.html\",\"project\":\"Dynamic Earth: Introduction to Physical Geography\",\"license\":\"cc-by-nc\",\"license_terms\":\"\"}]","CANDELA_OUTCOMES_GUID":"","pb_show_title":"on","pb_short_title":"","pb_subtitle":"","pb_authors":[],"pb_section_license":"cc-by-nc"},"chapter-type":[],"contributor":[],"license":[58],"class_list":["post-284","chapter","type-chapter","status-publish","hentry","license-cc-by-nc"],"part":138,"_links":{"self":[{"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/pressbooks\/v2\/chapters\/284","targetHints":{"allow":["GET"]}}],"collection":[{"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/pressbooks\/v2\/chapters"}],"about":[{"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/wp\/v2\/types\/chapter"}],"author":[{"embeddable":true,"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/wp\/v2\/users\/5"}],"version-history":[{"count":3,"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/pressbooks\/v2\/chapters\/284\/revisions"}],"predecessor-version":[{"id":859,"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/pressbooks\/v2\/chapters\/284\/revisions\/859"}],"part":[{"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/pressbooks\/v2\/parts\/138"}],"metadata":[{"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/pressbooks\/v2\/chapters\/284\/metadata\/"}],"wp:attachment":[{"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/wp\/v2\/media?parent=284"}],"wp:term":[{"taxonomy":"chapter-type","embeddable":true,"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/pressbooks\/v2\/chapter-type?post=284"},{"taxonomy":"contributor","embeddable":true,"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/wp\/v2\/contributor?post=284"},{"taxonomy":"license","embeddable":true,"href":"https:\/\/courses.lumenlearning.com\/suny-earthscience\/wp-json\/wp\/v2\/license?post=284"}],"curies":[{"name":"wp","href":"https:\/\/api.w.org\/{rel}","templated":true}]}}