| Ultramafic refers to the extremely mafic rocks composed of mostly olivine and some pyroxene which have even more magnesium and iron and even less silica. These rocks are rare on the surface, but make up peridotite, the rock of the upper mantle. It is poor in silica, in the 40% or less range. Show
On the figure above, the top row has both plutonic and volcanic igneous rocks arranged in a continuous spectrum from felsic on the left to intermediate, mafic, and ultramafic toward the right. Rhyolite thus refers to the volcanic and felsic igneous rocks, and granite thus refer to intrusive and felsic igneous rocks. Andesite and diorite likewise refer to extrusive and intrusive intermediate rocks (with dacite and granodiorite applying to those rocks with composition between felsic and intermediate). Basalt and gabbro are the extrusive and intrusive names for mafic igneous rocks, and peridotite is ultramafic, with komatiite as the fine-grained extrusive equivalent. Komatiite is a rare rock because volcanic material that comes direct from the mantle is not common, although some examples can be found in ancient Archean rocks. Nature rarely has sharp boundaries and the classification and naming of rocks often imposes what appear to be sharp boundary names onto a continuous spectrum.  Aphanitic/Phaneritic Rock Types with imagesFelsic Composition Gabbro is a coarse-grained mafic igneous rock, made with mainly mafic minerals like pyroxene and only minor plagioclase. Because mafic lava is more mobile, it is less common than basalt. Gabbro is a major component of the lower oceanic crust. Basalt is a fine-grained mafic igneous rock. It is commonly vesicular and aphanitic. When porphyritic, it often has either olivine or plagioclase phenocrysts. Basalt is the main rock which is formed at mid-ocean ridges, and is therefore the most common rock on the Earth’s surface, making up the entirety of the ocean floor (except where covered by sediment).4.1.3 Igneous Rock BodiesIgneous rocks are common in the geologic record, but surprisingly, it is the intrusive rocks that are more common. Extrusive rocks, because of their small crystals and glass, are less durable. Plus, they are, by definition, exposed to the elements of erosion immediately. Intrusive rocks, forming underground with larger, stronger crystals, are more likely to last. Therefore, most landforms and rock groups that owe their origin to igneous rocks are intrusive bodies. A significant exception to this is active volcanoes, which are discussed in a . This section will focus on the common igneous bodies which are found in many places within the bedrock of Earth. When magma intrudes into a weakness like a crack or fissure and solidifies, the resulting cross-cutting feature is called a dike (sometimes spelled dyke). Because of this, dikes are often vertical or at an angle relative to the pre-existing rock layers that they intersect. Dikes are therefore discordant intrusions, not following any layering that was present. Dikes are important to geologists, not only for the study of igneous rocks themselves but also for dating rock sequences and interpreting the geologic history of an area. The dike is younger than the rocks it cuts across and, as discussed in the chapter on Geologic Time (Chapter 7), may be used to assign actual numeric ages to sedimentary sequences, which are notoriously difficult to age date. Sills are another type of intrusive structure. A sill is a concordant intrusion that runs parallel to the sedimentary layers in the country rock. They are formed when magma exploits a weakness between these layers, shouldering them apart and squeezing between them. As with dikes, sills are younger than the surrounding layers and may be radioactively dated to study the age of sedimentary strata. A magma chamber is a large underground reservoir of molten rock. The path of rising magma is called a diapir. The processes by which a diapir intrudes into the surrounding native or country rock are not well understood and are the subject of ongoing geological inquiry. For example, it is not known what happens to the pre-existing country rock as the diapir intrudes. One theory is the overriding rock gets shouldered aside, displaced by the increased volume of magma. Another is the native rock is melted and consumed into the rising magma or broken into pieces that settle into the magma, a process known as stoping. It has also been proposed that diapirs are not a real phenomenon, but just a series of dikes that blend into each other. The dikes may be intruding over millions of years, but since they may be made of similar material, they would be appearing to be formed at the same time. Regardless, when a diapir cools, it forms an mass of intrusive rock called a pluton. Plutons can have irregular shapes, but can often be somewhat round. Laccoliths are blister-like, concordant intrusions of magma that form between sedimentary layers. The Henry Mountains of Utah are a famous topographic landform formed by this process. Laccoliths bulge upwards; a similar downward-bulging intrusion is called a lopolith. Click on the plus signs the illustration for descriptions of several igneous features. /5
4.1 Did I Get It? Take this quiz to check your comprehension of this section. Click directly on the answer button, not on the answer bar. 1 / 5 1. What causes igneous rocks to develop a fine-grained (aphanitic) texture? 1. Very high temperatures 2. Slow cooling 3. Fast cooling 4. Very high pressures 5. Lots of volatiles
Incorrect. Fine grain (aphanitic) igneous rocks cool rapidly on the surface. Correct! Fine grain (aphanitic) igneous rocks cool rapidly on the surface. 2 / 5 2. Where do igneous rocks with a coarse-grained (phaneritic) texture form? 1. on top of the surface. 2. deep under the surface. 3. Submarine lava flows 4. on top of the surface after being ejected into the air. 5. close to the surface but also just below it.
Incorrect. Phaneritic (coarse grain) igneous rocks cool slowly deep underground. Correct! Phaneritic (coarse grain) igneous rocks cool slowly deep underground. 3 / 5 3. Which rock composition has the most amount of iron and magnesium? 1. felsic 2. mafic 3. intermediate 4. ultramafic
Incorrect. Iron and magnesium decrease in the transition from ultramafic to felsic. Correct! Iron and magnesium decrease in the transition from ultramafic to felsic. 4 / 5 4. How does the silica content affect the behavior of magma? 1. Higher silica makes the magma more viscous 2. Higher silica makes the magma cool faster. 3. Higher silica makes the magma flow easier 4. Higher silica makes the magma have more carbon. 5. Higher silica makes the magma have less volatiles.
Incorrect. Increasing silica in the transition from ultramafic to felsic composition makes the magma more viscous. Correct! Increasing silica in the transition from ultramafic to felsic composition makes the magma more viscous. 5 / 5 5. A basaltic intrusion that cuts across layers of sedimentary rocks is called a _______. 1. stock 2. laccolith 3. sill 4. dike 5. batholith
Incorrect. A dike is an intrusion that cuts across sedimentary layers. Correct! A dike is an intrusion that cuts across sedimentary layers. Your score is 0% Restart quiz 4.2 Bowen’s Reaction SeriesIn the figure, the righthand column lists the four groups of igneous rock from top to bottom: ultramafic, mafic, intermediate, and felsic. The down-pointing arrow on the far right shows increasing amounts of silica, sodium, aluminum, and potassium as the mineral composition goes from ultramafic to felsic. The up-pointing arrow shows increasing ferromagnesian components, specifically iron, magnesium, and calcium. To the far left of the diagram is a temperature scale. Minerals near the top of diagram, such as olivine and anorthite (a type of plagioclase), crystallize at higher temperatures. Minerals near the bottom, such as quartz and muscovite, crystalize at lower temperatures. The most important aspect of Bowen’s Reaction Series is to notice the relationships between minerals and temperature. Norman L. Bowen (1887-1956) was an early 20th Century geologist who studied igneous rocks. He noticed that in igneous rocks, certain minerals always occur together and these mineral assemblages exclude other minerals. Curious as to why, and with the hypothesis in mind that it had to do with the temperature at which the rocks cooled, he set about conducting experiments on igneous rocks in the early 1900s. He conducted experiments on igneous rock—grinding combinations of rocks into powder, sealing the powders into metal capsules, heating them to various temperatures, and then cooling them. When he opened the quenched capsules, he found a glass surrounding mineral crystals that he could identify under his petrographic microscope. The results of many of these experiments, conducted at different temperatures over a period of several years, showed that the common igneous minerals crystallize from magma at different temperatures. He also saw that minerals occur together in rocks with others that crystallize within similar temperature ranges, and never crystallize with other minerals. This relationship can explain the main difference between mafic and felsic igneous rocks. Mafic igneous rocks contain more mafic minerals, and therefore, crystallize at higher temperatures than felsic igneous rocks. This is even seen in lava flows, with felsic lavas erupting hundreds of degrees cooler than their mafic counterparts. Bowen’s work laid the foundation for understanding igneous petrology (the study of rocks) and resulted in his book, The Evolution of the Igneous Rocks in 1928. /3
4.2 Did I Get It? Take this quiz to check your comprehension of this section. Click directly on the answer button, not on the answer bar. 1 / 3 1. Examine Bowen’s Reaction Series diagram. If a rock containes amphibole, potassium feldspar (orthoclase), and quartz, if the rock is heated, which mineral would melt first? 1. potassium feldspar (orthoclase) 2. quartz 3. • None. The melting point of these can’t be reached 4. amphibole
Incorrect. The Bowen diagram shows that quartz both crystallizes from cooling magma and melts from heated rock at the lowest temperature. Correct! The Bowen diagram shows that quartz both crystallizes from cooling magma and melts from heated rock at the lowest temperature. 2 / 3 2. Examine Bowen’s Reaction Series diagram. Which mineral has the highest temperature of crystallization? 1. olivine 2. Mica 3. quartz 4. k-spar 5. pyroxene
Incorrect. The Bowen diagram shows that olivine both crystallizes from cooling magma and melts from heated rock at the highest temperature. Correct! The Bowen diagram shows that olivine both crystallizes from cooling magma and melts from heated rock at the highest temperature. 3 / 3 3. Examine Bowen’s Reaction Series diagram. As a felsic magma cools, which mineral would be the last to crystallize? 1. biotite 2. muscovite 3. k-spar 4. olivine 5. quartz
Incorrect. The Bowen diagram shows that quartz both crystallizes from cooling magma and melts from heated rock at the lowest temperature. Correct! The Bowen diagram shows that quartz both crystallizes from cooling magma and melts from heated rock at the lowest temperature. Your score is 0% Restart quiz 4.3 Magma GenerationMagma and lava contain three components: melt, solids, and volatiles. The melt is made of ions from minerals that have liquefied. The solids are made of crystallized minerals floating in the liquid melt. These may be minerals that have already cooled Volatiles are gaseous components—such as water vapor, carbon dioxide, sulfur, and chlorine—dissolved in the magma. The presence and amount of these three components affect the physical behavior of the magma and will be discussed more below. 4.3.1 Geothermal GradientBelow the surface, the temperature of the Earth rises. This heat is caused by residual heat left from the formation of Earth and ongoing radioactive decay. The rate at which temperature increases with depth is called the geothermal gradient. The average geothermal gradient in the upper 100 km (62 mi) of the crust is about 25°C per kilometer of depth. So for every kilometer of depth, the temperature increases by about 25°C. The temperature at 100 km (62 mi) deep is about 1,200°C (2,192°F). At bottom of the crust, 35 km (22 mi) deep, the pressure is about 10,000 bars. A bar is a measure of pressure, with 1 bar being normal atmospheric pressure at sea level. At these pressures and temperatures, the crust and mantle are solid. To a depth of 150 km (93 mi), the geothermal gradient line stays to the left of the solidus line. This relationship continues through the mantle to the core-mantle boundary, at 2,880 km (1,790 mi). The solidus line slopes to the right because the melting temperature of any substance depends on pressure. The higher pressure created at greater depth increases the temperature needed to melt rock. In another example, at sea level with an atmospheric pressure close to 1 bar, water boils at 100°C. But if the pressure is lowered, as shown on the video below, water boils at a much lower temperature. There are three principal ways rock behavior crosses to the right of the green solidus line to create molten magma: 1) decompression melting caused by lowering the pressure, 2) flux melting caused by adding volatiles (see more below), and 3) heat-induced melting caused by increasing the temperature. The Bowen’s Reaction Series shows that minerals melt at different temperatures. Since magma is a mixture of different minerals, the solidus boundary is more of a fuzzy zone rather than a well-defined line; some minerals are melted and some remain solid. This type of rock behavior is called partial melting and represents real-world magmas, which typically contain solid, liquid, and volatile components. The figure below uses P-T diagrams to show how melting can occur at three different plate tectonic settings. The green line is called the solidus, the melting point temperature of the rock at that pressure. Setting A is a situation (called “normal”) in the middle of a stable plate in which no magma is generated. In the other three situations, rock at a lettered location with a temperature at the geothermal gradient is moved to a new P-T situation on the diagram. This shift is indicated by the arrow and its temperature relative to the solidus is shown by the red line. Partial melting occurs where the red line temperature of the rock crosses the green solidus on the diagram. Setting B is at a mid-ocean ridge (decompression melting) where reduction of pressure carries the rock at its temperature across the solidus. Setting C is a hotspot where decompression melting plus addition of heat carries the rock across the solidus, and setting D is a subduction zone where a process called flux melting takes place where the solidus (melting point) is actually shifted to below the temperature of the rock. Graphs A-D below, along with the side view of the Earth’s layers in various tectonic settings (see figure), show how melting occurs in different situations. Graph A illustrates a normal situation, located in the middle of a stable plate, where no melted rock can be found. The remaining three graphs illustrate rock behavior relative to shifts in the geothermal gradient or solidus lines. Partial melting occurs when the geothermal gradient line crosses the solidus line. Graph B illustrates behavior of rock located at a mid-ocean ridge, labeled X in the graph and side view. Reduced pressure shifts the geotherm to the right of the solidus, causing decompression melting. Graph C and label Y illustrate a hotspot situation. Decompression melting, plus an addition of heat, shifts the geotherm across the solidus. Graph D and label Z show a subduction zone, where an addition of volatiles lowers the melting point, shifting the solidus to the left of the geothermal gradient. B, C, and D all show different ways the Earth produces intersections of the geothermal gradient and the solidus, which results in melting each time. 4.3.2 Decompression Melting4.3.3 Flux MeltingFlux melting or fluid-induced melting occurs in island arcs and subduction zones when volatile gases are added to mantle material (see figure: graph D, label Z). Flux-melted magma produces many of the volcanoes in the circum-Pacific subduction zones, also known as the Ring of Fire. The subducting slab contains oceanic lithosphere and hydrated minerals. As covered in Chapter 2, these hydrated forms are created when water ions bond with the crystal structure of silicate minerals. As the slab descends into the hot mantle, the increased temperature causes the hydrated minerals to emit water vapor and other volatile gases, which are expelled from the slab like water being squeezed out of a sponge. The volatiles dissolve into the overlying asthenospheric mantle and decrease its melting point. In this situation the applied pressure and temperature have not changed, the mantle’s melting point has been lowered by the addition of volatile substances. The previous figure (graph D) shows the green solidus line shifting to the left of and below the red geothermal gradient line, and melting begins. This is analogous to adding salt to an icy roadway. The salt lowers the freezing temperature of the solid ice so it turns into liquid water. 4.3.4 Heat-Induced MeltingHeat-induced melting, transforming solid mantle into liquid magma by simply applying heat, is the least common process for generating magma (see figure: graph C, label Y). Heat-induced melting occurs at a mantle plumes or hotspots. The rock surrounding the plume is exposed to higher temperatures, the geothermal gradient crosses to the right of the green solidus line, and the rock begins to melt. The mantle plume includes rising mantle material, meaning some decompression melting is occurring as well. A small amount of magma is also generated by intense regional metamorphism (see Chapter 6). This magma becomes a hybrid metamorphic-igneous rock called migmatite. /3
4.3 Did I Get It? Take this quiz to check your comprehension of this section. Click directly on the answer button, not on the answer bar. 1 / 3 1. What is the process by which decompression melting produces magma at divergent plate boundaries? 1. addition of fluid at constant pressure 2. reduction of pressure at constant temperature 3. addition of heat at constant depth 4. Increase of temperature at constant pressure
Incorrect. Decompression melting takes place when pressure is reduced on rising asthenospheric material which remains at the same temperature at divergent boundaries. Correct! Decompression melting takes place when pressure is reduced on rising asthenospheric material which remains at the same temperature at divergent boundaries. 2 / 3 2. If volatiles such as water vapor and carbon dioxide are added to a rock, what will happen to the melting temperature? 1. The melting temperature will not change. It is dependent on the pressure. 2. • The rock will expand increasing the pressure. 3. The melting temperature of a rock will decrease. 4. The melting temperature of a rock will increase.
Incorrect. Volatiles added to hot rock act as a flux reducing the melting point and causing the rock to melt at that same temperature. Correct! Volatiles added to hot rock act as a flux reducing the melting point and causing the rock to melt at that same temperature. 3 / 3 3. What does a P-T diagram of the mantle show? 1. It shows how the mantle is liquid magma under the surface. 2. It shows how pressure and temperature increase with depth. 3. It shows how temperature increases but pressure decreases with depth. 4. It shows how Celsius and kilobars change. 5. It shows that rocks in the subsurface can never melt.
Incorrect. A P-T diagram plots temperature against pressure, both of which increase with depth. Correct! A P-T diagram plots temperature against pressure, both of which increase with depth. Your score is 0% Restart quiz 4.4 Partial Melting and CrystallizationEven though all magmas originate from similar mantle rocks, and start out as similar magma, other things, like partial melting and crystallization processes like magmatic differentiation, can change the chemistry of the magma. This explains the wide variety of resulting igneous rocks that are found all over Earth. 4.4.1 Partial MeltingBecause the mantle is composed of many different minerals, it does not melt uniformly. As minerals with lower melting points turn into liquid magma, those with higher melting points remain as solid crystals. This is known as partial melting. As magma slowly rises and cools into solid rock, it undergoes physical and chemical changes in a process called magmatic differentiation. According to Bowen’s Reaction Series (), each mineral has a unique melting and crystallization temperature. Since most rocks are made of many different minerals, when they start to melt, some minerals begin melting sooner than others. This is known as partial melting, and creates magma with a different composition than the original mantle material. The most important example occurs as magma is generated from mantle rocks (as discussed in ). The chemistry of mantle rock (peridotite) is ultramafic, low in silicates and high in iron and magnesium. When peridotite begins to melt, the silica-rich portions melt first due to their lower melting point. If this continues, the magma becomes increasingly silica-rich, turning ultramafic mantle into mafic magma, and mafic mantle into intermediate magma. The magma rises to the surface because it is more buoyant than the mantle. 4.4.2 Crystallization and Magmatic DifferentiationLiquid magma is less dense than the surrounding solid rock, so it rises through the mantle and crust. As magma begins to cool and crystallize, a process known as magmatic differentiation changes the chemistry of the resultant rock towards a more felsic composition. This happens via two main methods: assimilation and fractionation. During assimilation, pieces of country rock with a different, often more felsic, composition are added to the magma. These solid pieces may melt, which changes the composition of the original magma. At times, the solid fragments may remain intact within the cooling magma and only partially melt. The unmelted country rocks within an igneous rock mass are called xenoliths. Xenoliths are also common in the processes of magma mixing and rejuvenation, two other processes that can contribute to magmatic differentiation. Magma mixing occurs when two different magmas come into contact and mix, though at times, the magmas can remain heterogeneous and create xenoliths, dikes, and other features. Magmatic rejuvenation happens when a cooled and crystallized body of rock is remelted and pieces of the original rock may remain as xenoliths. Much of the continental lithosphere is felsic (i.e. granitic), and normally more buoyant than the underlying mafic/ultramafic mantle. When mafic magma rises through thick continental crust, it does so slowly, more slowly than when magma rises through oceanic plates. This gives the magma lots of time to react with the surrounding country rock. The mafic magma tends to assimilate felsic rock, becoming more silica-rich as it migrates through the lithosphere and changing into intermediate or felsic magma by the time it reaches the surface. This is why felsic magmas are much more common within continents. /5
4.4 Did I Get It? Take this quiz to check your comprehension of this section. Click directly on the answer button, not on the answer bar. 1 / 5 1. As magma travels up from the asthenosphere through the lithosphere into continental crust, how will fractional crystallization change the chemistry of an ultramafic magma? 1. • The ultramafic magma will lose sodium. 2. The ultramafic magma will become more iron-rich. 3. The ultramafic magma will become more mafic. 4. The ultramafic magma will become depleted in potassium.
Incorrect. Referring to the Bowen diagram and fractional crystallization, the ultramafic magma will become more mafic. Correct! Referring to the Bowen diagram and fractional crystallization, the ultramafic magma will become more mafic. 2 / 5 2. Unmelted pieces of country rock incorporated within the igneous rock mass are called _______. 1. assimilation material 2. xenoliths 3. partial melting 4. assimilation
Incorrect. Xenoliths are bits of country rock that are incorporated within a mass of igneous rock. Correct! Xenoliths are bits of country rock that are incorporated within a mass of igneous rock. 3 / 5 3. Crystal settling would be another name for ______. 1. xenolith formation 2. assimilation 3. Bowen's Reaction Series 4. fractional crystallization
Incorrect. Fractional crystallization by crystals settling out under gravity is one way that magmas can change in composition while cooling. Correct! Fractional crystallization by crystals settling out under gravity is one way that magmas can change in composition while cooling. 4 / 5 4. The crystallization process in which a rising magma diapir incorporates some of the surrounding country rock so that the chemistry of the magma changes is called _____. 1. assimilation 2. fractional crystallization 3. xenolith 4. lower density magma rising through higher density country rock
Incorrect. Assimilation is the process by which rising magma incorporates country rock and composition changes. Correct! Assimilation is the process by which rising magma incorporates country rock and composition changes. 5 / 5 5. Partially melting an ultramafic rock produces a magma with a(n) _________ composition. 1. mafic 2. ultramafic 3. felsic 4. intermediate
Incorrect. Partial melting produces a magma a step lower on the Bowen diagram than the rock from which it melts. Correct! Partial melting produces a magma a step lower on the Bowen diagram than the rock from which it melts. Your score is 0% Restart quiz 4.5 VolcanismWhen magma emerges onto the Earth’s surface, the molten rock is called lava. A volcano is a type of land formation created when lava solidifies into rock. Volcanoes have been an important part of human society for centuries, though their understanding has greatly increased as our understanding of plate tectonics has made them less mysterious. This section describes volcano location, type, hazards, and monitoring. 4.5.1. Distribution and TectonicsMost volcanoes are interplate volcanoes. Interplate volcanoes are located at active plate boundaries created by volcanism at mid-ocean ridges, subduction zones, and continental rifts. The prefix “inter-“ means between. Some volcanoes are intraplate volcanoes. The prefix “intra-“ means within, and intraplate volcanoes are located within tectonic plates, far removed from plate boundaries. Many intraplate volcanoes are formed by hotspots. Volcanoes at Mid-Ocean RidgesWhen basaltic lava erupts underwater it emerges in small explosions and/or forms pillow-shaped structures called pillow basalts. These seafloor eruptions enable entire underwater ecosystems to thrive in the deep ocean around mid-ocean ridges. This ecosystem exists around tall vents emitting black, hot mineral-rich water called deep-sea hydrothermal vents, also known as black smokers. Volcanoes at Subduction ZonesThe second most commonly found location for volcanism is adjacent to subduction zones, a type of convergent plate boundary (see ). The process of subduction expels water from hydrated minerals in the descending slab, which causes flux melting in the overlying mantle rock. Because subduction volcanism occurs in a volcanic arc, the thickened crust promotes partial melting and magma differentiation. These evolve the mafic magma from the mantle into more silica-rich magma. The Ring of Fire surrounding the Pacific Ocean, for example, is dominated by subduction-generated eruptions of mostly silica-rich lava; the volcanoes and plutons consist largely of intermediate-to-felsic rock such as andesite, rhyolite, pumice, and tuff. Volcanoes at Continental RiftsHotspotsSince most mantle plumes are located beneath the oceanic lithosphere, the early stages of intraplate volcanism typically take place underwater. Over time, basaltic volcanoes may build up from the sea floor into islands, such as the Hawaiian Islands. Where a hotspot is found under a continental plate, contact with the hot mafic magma may cause the overlying felsic rock to melt and mix with the mafic material below, forming intermediate magma. Or the felsic magma may continue to rise, and cool into a granitic batholith or erupt as a felsic volcano. The Yellowstone caldera is an example of hotspot volcanism that resulted in an explosive eruption. A zone of actively erupting volcanism connected to a chain of extinct volcanoes indicates intraplate volcanism located over a hotspot. These volcanic chains are created by the overriding oceanic plate slowly moving over a hotspot mantle plume. These chains are seen on the seafloor and continents and include volcanoes that have been inactive for millions of years. The Hawaiian Islands on the Pacific Oceanic plate are the active end of a long volcanic chain that extends from the northwest Pacific Ocean to the Emperor Seamounts, all the way to the to the subduction zone beneath the Kamchatka Peninsula. The overriding North American continental plate moved across a mantle plume hotspot for several million years, creating a chain of volcanic calderas that extends from Southwestern Idaho to the presently active Yellowstone caldera in Wyoming. Two three-minute videos (below) illustrates hotspot volcanoes. 4.5.2 Volcano Features and TypesThere are several different types of volcanoes based on their shape, eruption style, magmatic composition, and other aspects. The figure shows the main features of a typical stratovolcano: 1) magma chamber, 2) upper layers of lithosphere, 3) the conduit or narrow pipe through which the lava erupts, 4) the base or edge of the volcano, 5) a sill of magma between layers of the volcano, 6) a diapir or feeder tube to the sill, 7) layers of tephra (ash) from previous eruptions, 8 & 9) layers of lava erupting from the vent and flowing down the sides of the volcano, 10) the crater at the top of the volcano, 11) layers of lava and tephra on (12), a parasitic cone. A parasitic cone is a small volcano located on the flank of a larger volcano such as Shastina on Mount Shasta. Kilauea sitting on the flank of Mauna Loa is not considered a parasitic cone because it has its own separate magma chamber, 13) the vents of the parasite and the main volcano, 14) the rim of the crater, 15) clouds of ash blown into the sky by the eruption; this settles back onto the volcano and surrounding land.The largest craters are called calderas, such as the Crater Lake Caldera in Oregon. Many volcanic features are produced by viscosity, a basic property of a lava. Viscosity is the resistance to flowing by a fluid. Low viscosity magma flows easily more like syrup, the basaltic volcanism that occurs in Hawaii on shield volcanoes. High viscosity means a thick and sticky magma, typically felsic or intermediate, that flows slowly, similar to toothpaste. Shield VolcanoTypically, shield volcano eruptions are not much of a hazard to human life—although non-explosive eruptions of Kilauea (Hawaii) in 2018 produced uncharacteristically large lavas that damaged roads and structures. Mauna Loa (see USGS page) and Kilauea (see USGS page) in Hawaii are examples of shield volcanoes. Shield volcanoes are also found in Iceland, the Galapagos Islands, Northern California, Oregon, and the East African Rift. The largest volcanic edifice in the Solar System is Olympus Mons on Mars. This (possibly extinct) shield volcano covers an area the size of the state of Arizona. This may indicate the volcano erupted over a hotspot for millions of years, which means Mars had little, if any, plate tectonic activity. Basaltic lava forms special landforms based on magma temperature, composition, and content of dissolved gases and water vapor. The two main types of basaltic volcanic rock have Hawaiian names—pahoehoe and aa. Pahoehoe might come from low-viscosity lava that flows easily into ropey strands. Aa (sometimes spelled a’a or ʻaʻā and pronounced “ah-ah”) is more viscous and has a crumbly blocky appearance. The exact details of what forms the two types of flows are still up for debate. Felsic lavas have lower temperatures and more silica, and thus are higher viscosity. These also form aa-style flows. Low-viscosity, fast-flowing basaltic lava tends to harden on the outside into a tube and continue to flow internally. Once lava flow subsides, the empty outer shell may be left as a lava tube. Lava tubes, with or without collapsed roofs, make famous caves in Hawaii, Northern California, the Columbia River Basalt Plateau of Washington and Oregon, El Malpais National Monument in New Mexico, and Craters of the Moon National Monument in Idaho. Fissures are cracks that commonly originate from shield-style eruptions. Lava emerging from fissures is typically mafic and very fluid. The 2018 Kiluaea eruption included fissures associated with the lava flows. Some fissures are caused by the volcanic seismic activity rather than lava flows. Some fissures are influenced by plate tectonics, such as the common fissures located parallel to the divergent boundary in Iceland. Cooling lava can contract into columns with semi-hexagonal cross sections called columnar jointing. This feature forms the famous Devils Tower in Wyoming, possibly an ancient volcanic vent from which the surrounding layers of lava and ash have been removed by erosion. Another well-known exposed example of columnar jointing is the Giant’s Causeway in Ireland. StratovolcanoA stratovolcano, also called a composite cone volcano, has steep flanks, a symmetrical cone shape, distinct crater, and rises prominently above the surrounding landscape. The term composite refers to the alternating layers of pyroclastic fragments like ash and bombs, and solidified lava flows of varying composition. Examples include Mount Rainier in Washington state and Mount Fuji in Japan. Stratovolcanoes usually have felsic to intermediate magma chambers, but can even produce mafic lavas. Stratovolcanoes have viscous lava flows and domes, punctuated by explosive eruptions. This produces volcanoes with steep flanks. Lava DomesLava domes are accumulations of silica-rich volcanic rock, such as rhyolite and obsidian. Too viscous to flow easily, the felsic lava tends to pile up near the vent in blocky masses. Lava domes often form in a vent within the collapsed crater of a stratovolcano, and grow by internal expansion. As the dome expands, the outer surface cools, hardens, and shatters, and spills loose fragments down the sides. Mount Saint Helens has a good example of a lava dome inside of a collapsed stratovolcano crater. Examples of stand-alone lava domes are Chaiten in Chile and Mammoth Mountain in California. CalderaCalderas are steep-walled, basin-shaped depressions formed by the collapse of a volcanic edifice into an empty magma chamber. Calderas are generally very large, with diameters of up to 25 km (15.5 mi). The term caldera specifically refers to a volcanic vent; however, it is frequently used to describe a volcano type. Caldera volcanoes are typically formed by eruptions of high-viscosity felsic lava having high volatiles content. Crater Lake, Yellowstone, and the Long Valley Caldera are good examples of this type of volcanism. The caldera at Crater Lake National Park in Oregon was created about 6,800 years ago when Mount Mazama, a composite volcano, erupted in a huge explosive blast. The volcano ejected large amounts of volcanic ash and rapidly drained the magma chamber, causing the top to collapse into a large depression that later filled with water. Wizard Island in the middle of the lake is a later resurgent lava dome that formed within the caldera basin. The Yellowstone volcanic system erupted three times in the recent geologic past—2.1, 1.3, and 0.64 million years ago—leaving behind three caldera basins. Each eruption created large rhyolite lava flows as well as pyroclastic flows that solidified into tuff formations. These extra-large eruptions rapidly emptied the magma chamber, causing the roof to collapse and form a caldera. The youngest of the three calderas contains most of Yellowstone National Park, as well as two resurgent lava domes. The calderas are difficult to see today due to the amount of time since their eruptions and subsequent erosion and glaciation. Yellowstone volcanism started about 17-million years ago as a hotspot under the North American lithospheric plate near the Oregon/Nevada border. As the plate moved to the southwest over the stationary hotspot, it left behind a track of past volcanic activities. Idaho’s Snake River Plain was created from volcanism that produced a series of calderas and lava flows. The plate eventually arrived at its current location in northwestern Wyoming, where hotspot volcanism formed the Yellowstone calderas. The Long Valley Caldera near Mammoth, California, is the result of a large volcanic eruption that occurred 760,000 years ago. The explosive eruption dumped enormous amounts of ash across the United States, in a manner similar to the Yellowstone eruptions. The Bishop Tuff deposit near Bishop, California, is made of ash from this eruption. The current caldera basin is 17 km by 32 km (10 mi by 20 mi), large enough to contain the town of Mammoth Lakes, major ski resort, airport, major highway, resurgent dome, and several hot springs. Cinder ConeCinder cones are small volcanoes with steep sides, and made of pyroclastic fragments that have been ejected from a pronounced central vent. The small fragments are called cinders and the largest are volcanic bombs. The eruptions are usually short-lived events, typically consisting of mafic lavas with a high content of volatiles. Hot lava is ejected into the air, cooling and solidifying into fragments that accumulate on the flank of the volcano. Cinder cones are found throughout western North America.
A recent and striking example of a cinder cone is the eruption near the village of Parícutin, Mexico that started in 1943. The cinder cone started explosively shooting cinders out of the vent in the middle of a farmer’s field. The volcanism quickly built up the cone to a height of over 90 m (300 ft) within a week, and 365 m (1,200 ft) within the first 8 months. After the initial explosive eruption of gases and cinders, basaltic lava poured out from the base of the cone. This is a common order of events for cinder cones: violent eruption, cone and crater formation, low-viscosity lava flow from the base. The cinder cone is not strong enough to support a column of lava rising to the top of the crater, so the lava breaks through and emerges near the bottom of the volcano. During nine years of eruption activity, the ashfall covered about 260 km2 (100 mi2) and destroyed the nearby town of San Juan. Flood BasaltsA rare volcanic eruption type, unobserved in modern times, is the flood basalt. Flood basalts are some of the largest and lowest viscosity types of eruptions known. They are not known from any eruption in human history, so the exact mechanisms of eruption are still mysterious. Some famous examples include the Columbia River Flood Basalts in Washington, Oregon, and Idaho, the Deccan Traps, which cover about 1/3 of the country of India, and the Siberian Traps, which may have been involved in the Earth’s largest mass extinction (see chapter 8). CarbonatitesArguably the most unusual volcanic activity are carbonatite eruptions. Only one actively erupting carbonatite volcano exists on Earth today, Ol Doinyo Lengai, in the East African Rift Zone of Tanzania. While all other volcanism on Earth originates from silicate-based magma, carbonatites are a product of carbonate-based magma and produce volcanic rocks containing greater than 50% carbonate minerals. Carbonatite lavas are very low viscosity and relatively cold for lava. The erupting lava is black, and solidifies to brown/grey rock that eventually turns white. These rocks are occasionally found in the geologic record and require special study to distinguish them from metamorphic marbles (see Chapter 6). They are mostly associated with continental rifting. Igneous rock types and related volcano types. Mid-ocean ridges and shield volcanoes represent more mafic compositions, and strato (composite) volcanoes generally represent a more intermediate or felsic composition and a convergent plate tectonic boundary. Note that there are exceptions to this generalized layout of volcano types and igneous rock composition. 4.5.3 Volcanic Hazards and MonitoringWhile the most obvious volcanic hazard is lava, the dangers posed by volcanoes go far beyond lava flows. For example, on May 18, 1980, Mount Saint Helens (Washington, United States) erupted with an explosion and landslide that removed the upper 400 m (1,300 ft) of the mountain. The initial explosion was immediately followed by a lateral blast, which produced a pyroclastic flow that covered nearly 600 km2 (230 mi2) of forest with hot ash and debris. The pyroclastic flow moved at speeds of 80-130 kph (50-80 mph), flattening trees and ejecting clouds of ash into the air. The USGS video provides an account of this explosive eruption that killed 57 people. In 79 AD, Mount Vesuvius, located near Naples, Italy, violently erupted sending a pyroclastic flow over the Roman countryside, including the cities of Herculaneum and Pompeii. The buried towns were discovered in an archeological expedition in the 18th century. Pompeii famously contains the remains (casts) of people suffocated by ash and covered by 10 feet (3 m) of ash, pumice lapilli, and collapsed roofs. Pyroclastic flowsThe most dangerous volcanic hazard are pyroclastic flows (video). These flows are a mix of lava blocks, pumice, ash, and hot gases between 200°C-700°C (400°F-1,300°F). The turbulent cloud of ash and gas races down the steep flanks at high speeds up to 193 kph (120 mph) into the valleys around composite volcanoes. Most explosive, silica-rich, high viscosity magma volcanoes such as composite cones usually have pyroclastic flows. The rock tuff and welded tuff is often formed from these pyroclastic flows. There are numerous examples of deadly pyroclastic flows. In 2014, the Mount Ontake pyroclastic flow in Japan killed 47 people. The flow was caused by magma heating groundwater into steam, which then rapidly ejected with ash and volcanic bombs. Some were killed by inhalation of toxic gases and hot ash, while others were struck by volcanic bombs. Two short videos below document eye-witness video of pyroclastic flows. In the early 1990s, Mount Unzen erupted several times with pyroclastic flows. The pyroclastic flow shown in this famous short video killed 41 people. In 1902, on the Caribbean Island Martinique, Mount Pelee erupted with a violent pyroclastic flow that destroyed the entire town of St. Pierre and killing 28,000 people in moments. Landslides and Landslide-Generated TsunamisThe steep and unstable flanks of a volcano can lead to slope failure and dangerous landslides. These landslides can be triggered by magma movement, explosive eruptions, large earthquakes, and/or heavy rainfall. During the 1980 Mount St. Helens eruption, the entire north flank of the volcano collapsed and released a huge landslide that moved at speeds of 160-290 kph (100-180 mph). If enough landslide material reaches the ocean, it may cause a tsunami. In 1792, a landslide caused by the Mount Unzen eruption reached the Ariaka Sea, generating a tsunami that killed 15,000 people (see USGS page). When Mount Krakatau in Indonesia erupted in 1883, it generated ocean waves that towered 40 m (131 ft) above sea level. The tsunami killed 36,000 people and destroyed 165 villages. TephraHot ash poses an immediate danger to people, animals, plants, machines, roads, and buildings located close to the eruption. Ash is fine grained (< 2mm) and can travel airborne long distances away from the eruption site. Heavy accumulations of ash can cause buildings to collapse. In people, it may cause respiratory issues like silicosis. Ash is destructive to aircraft and automobile engines, which can disrupt transportation and shipping services. In 2010, the Eyjafjallajökull volcano in Iceland emitted a large ash cloud into the upper atmosphere, causing the largest air-travel disruption in northern Europe since World War II. No one was injured, but the service disruption was estimated to have cost the world economy billions of dollars. Volcanic GasesAs magma rises to the surface the confining pressure decreases, and allows dissolved gases to escape into the atmosphere. Even volcanoes that are not actively erupting may emit hazardous gases, such as carbon dioxide (CO2), sulfur dioxide (SO2), hydrogen sulfide (H2S), and hydrogen halides (HF, HCl, or HBr). Carbon dioxide tends to sink and accumulate in depressions and basins. In volcanic areas known to emit carbon dioxide, low-lying areas may trap hazardous concentrations of this colorless and odorless gas. The Mammoth Mountain Ski Resort in California, is located within the Long Valley Caldera, is one such area of carbon dioxide-producing volcanism. In 2006, three ski patrol members died of suffocation caused by carbon dioxide after falling into a snow depression near a fumarole (info). In rare cases, volcanism may create a sudden emission of gases without warning. Limnic eruptions (limne is Greek for lake), occur in crater lakes associated with active volcanism. The water in these lakes is supercharged with high concentrations of dissolved gases. If the water is physically jolted by a landslide or earthquake, it may trigger an immediate and massive release of gases out of solution. An analogous example would be what happens to vigorously shaken bottle of carbonated soda when the cap is opened. An infamous limnic eruption occurred in 1986 at Lake Nyos, Cameroon. Almost 2,000 people were killed by a massive release of carbon dioxide. LaharsLahar is an Indonesian word and is used to describe a volcanic mudflow that forms from rapidly melting snow or glaciers. Lahars are slurries resembling wet concrete, and consist of water, ash, rock fragments, and other debris. These mudflows flow down the flanks of volcanoes or mountains covered with freshly-erupted ash and on steep slopes can reach speeds of up to 80 kph (50 mph). Several major cities, including Tacoma, are located on prehistoric lahar flows that extend for many kilometers across the flood plains surrounding Mount Rainier in Washington (see map). A map of Mount Baker in Oregon shows a similar potential hazard for lahar flows (see map). A tragic scenario played out recently, in 1985, when a lahar from the Nevado del Ruiz volcano in Colombia buried the town of Armero and killed an estimated 23,000 people. MonitoringGeologists use various instruments to detect changes or indications that an eruption is imminent. The three videos show different types of volcanic monitoring used to predict eruptions 1) earthquake activity; 2) increases in gas emission; and 3) changes in land surface orientation and elevation. One video shows how monitoring earthquake frequency, especially special vibrational earthquakes called harmonic tremors, can detect magma movement and possible eruption. Another video shows how gas monitoring may be used to predict an eruption. A rapid increase of gas emission may indicate magma that is actively rising to surface and releasing dissolved gases out of solution, and that an eruption is imminent. The last video shows how a GPS unit and tiltmeter can detect land surface changes, indicating the magma is moving underneath it. /5
4.5 Did I Get It? Take this quiz to check your comprehension of this section. Click directly on the answer button, not on the answer bar. 1 / 5 1. Explosive silica-rich volcanoes will be located mostly at ______. 1. convergent plate boundaries with subduction zones 2. divergent boundaries of the mid-ocean ridge 3. divergent boundaries of the East African Rift 4. convergent plate boundaries with continental to continental plate collisions
Incorrect. Explosive volcanism is commonly associated with the Ring of Fire which is a ring of subduction zones. Correct! Explosive volcanism is commonly associated with the Ring of Fire which is a ring of subduction zones. 2 / 5 2. A _______ volcano has steep flanks, symmetrical cone shapes, distinct crater at the top, and a silica-rich magma that results in an explosive eruption style. 1. flood basalt 2. stratovolcano (or composite volcano) 3. shield volcano 4. caldera 5. cinder cone
Incorrect. Stratovolcanoes are symmetrical and picturesque volcanic mountains resulting from explosive silica-rich magmas. Correct! Stratovolcanoes are symmetrical and picturesque volcanic mountains resulting from explosive silica-rich magmas. 3 / 5 3. Deep-sea hydrothermal vents (black smokers) are most commonly located at what plate boundary? 1. convergent boundaries with subduction zones 2. divergent boundaries of the mid-ocean ridge 3. divergent boundaries of the East African Rift 4. convergent boundaries with oceanic to oceanic plate subduction
Incorrect. Black smokers are associated with the mid-ocean ridge. Correct! Black smokers are associated with the mid-ocean ridge. 4 / 5 4. A __________ is a volcanic hazard arising from a collapsing eruption column that runs downhill at high speeds (>100 mph). These are associated with explosive eruptions and a mix of lava lapilli, pumice, ash, and hot gases. 1. rain composed of acid 2. pyroclastic flow 3. lapilli flow 4. ash and lahar flow
Incorrect. A pyroclastic flow is hot gases containing ash and small rock particles called lapilli that rush at tremendous speeds down flanks of volcanoes. Correct! A pyroclastic flow is hot gases containing ash and small rock particles called lapilli that rush at tremendous speeds down flanks of volcanoes. 5 / 5 5. The largest type of volcano is called a _______ volcano and is characterized by broad, low-angle flanks, a small vent or groups of vents at the top, and basaltic magma. 1. caldera 2. stratovolcano (composite cone) 3. lava dome 4. cinder cone 5. shield volcano
Incorrect. Shield volcanoes are the largest type with these characteristics. Correct! Shield volcanoes are the largest type with these characteristics. Your score is 0% Restart quiz SummaryIgneous rock is divided into two major groups: intrusive rock that solidifies from underground magma, and extrusive rock formed from lava that erupts and cools on the surface. Magma is generated from mantle material at several plate tectonics situations by three types of melting: decompression melting, flux melting, or heat-induced melting. Magma composition is determined by differences in the melting temperatures of the mineral components (Bowen’s Reaction Series). The processes affecting magma composition include partial melting, magmatic differentiation, assimilation, and collision. Volcanoes come in a wide variety of shapes and sizes, and are classified by a multiple factors, including magma composition, and plate tectonic activity. Because volcanism presents serious hazards to human civilization, geologists carefully monitor volcanic activity to mitigate or avoid the dangers it presents. /10
Chapter 4 Review Take this quiz to check your comprehension of this chapter. Click directly on the answer button, not on the answer bar. 1 / 10 1. Which of these is NOT a means by which magmas are generated in the Earth? 1. Flux melting 2. Added heat melting 3. Decompression melting 4. Liquid melting
Incorrect. Liquid melting is not a means by which magmas are generated. Correct! Liquid melting is not a means by which magmas are generated. 2 / 10 2. A rock with aphanitic texture and dark color is best identified as a _______________. 1. granite 2. diorite 3. basalt 4. gabbro 5. pegmatite
Incorrect. Since mineral composition of aphanitic rocks is difficult without special equipment, dark color is associated with mafic composition and basalt is a reasonable identification. Correct! Since mineral composition of aphanitic rocks is difficult without special equipment, dark color is associated with mafic composition and basalt is a reasonable identification. 3 / 10 3. A pegmatite is characterized by __________ that forms from __________. 1. Pockets of fluid; volatiles extruded from cooling magma 2. Medieval window panes; demands of the very wealthy 3. Very large crystals of felsic composition; very slow cooling of residual material expelled from cooling magma 4. Lots of quartz; rapid cooling of felsic magma 5. Low silica; intrusions of ultramafic magmas
Incorrect. Pegmatites are composed of very large mineral crystals, commonly of felsic composition, that form from residual material expelled from cooling magma. Correct! Pegmatites are composed of very large mineral crystals, commonly of felsic composition, that form from residual material expelled from cooling magma. 4 / 10 4. Which of these relatively recent volcanic eruptions formed a caldera? 1. Mt. St. Helens 2. Mauna Loa 3. Mt. Fuji 4. Yellowstone 5. Paracutín
Incorrect. Within the last million years or so, the Yellowstone eruption formed a caldera that contains Yellowstone Lake. Correct! Within the last million years or so, the Yellowstone eruption formed a caldera that contains Yellowstone Lake. 5 / 10 5. Bowen’s Reaction Series has been expressed as a Y-shaped diagram containing how many minerals? 1. 8 2. 4 3. 6 4. 9 5. 5
Incorrect. The Bowen diagram is a simple Y-shape with 8 minerals and a temperature scale. Correct! The Bowen diagram is a simple Y-shape with 8 minerals and a temperature scale. 6 / 10 6. A porphyritic igneous rock has what defining characteristic? 1. Phaneritic crystals 2. Aphanitic crystals 3. Larger crystals in a finer grained groundmass 4. Lots of quartz 5. Very low silica content
Incorrect. Porphyritic rocks have larger crystals (phenocrysts) in a fine grained groundmass representing different stages of cooling. Correct! Porphyritic rocks have different larger crystals (phenocrysts) in a fine grained groundmass representing different stages of cooling. 7 / 10 7. Why does partial melting occur? 1. Because some minerals have iron and magnesium 2. Because the mantle is solid, only some minerals can melt 3. Because some minerals are harder than others 4. Because some minerals have lower melting points than others 5. Because some minerals have 3D structures
Incorrect. Partial melting occurs when minerals with a lower melting point melt out of a solid rock that also contains minerals with a higher melting point that remain solid. Correct! Partial melting occurs when minerals with a lower melting point melt out of a solid rock that also contains minerals with a higher melting point that remain solid. 8 / 10 8. What does the Bowen Reaction Series show about the mineral composition of igneous rocks? 1. Calcium rich plagioclase is the first mineral to melt as a rock is heated. 2. Aphanitic rocks are always mafic in composition. 3. The minerals in igneous rocks form in separate groups that depend on the temperature at which they crystallize. 4. Peridotite in the mantle is usually molten. 5. Pyroxene and orthoclase are commonly found together.
Incorrect. The beauty of Bowen’s work is showing that igneous minerals always form in specific mineral groupings depending on their temperature of crystallization. Correct! The beauty of Bowen’s work is showing that igneous minerals always form in specific mineral groupings depending on their temperature of crystallization. 9 / 10 9. What kind of volcanoes make up the Hawaiian Island Chain? 1. stratovolcanoes 2. shield volcanoes 3. cinder cones 4. calderas 5. lava domes
Incorrect. They are shield volcanoes that build up to tall mountains on the sea floor extending above sea level by repeating lava eruptions over many millennia. How is magma generated at divergent plate boundaries?plates move apart at a divergent plate boundary, the release of pressure produces partial melting of the underlying mantle. This molten material, known as magma, is basaltic in composition and is buoyant. As a result, it wells up from below and cools close to the surface to generate new crust.…
How is magma generated at divergent boundaries quizlet?Divergent boundaries cause magma because as the tectonic plates pull apart and mantle rock rises to fill the space the pressure on the mantle rock is reduced and the lowering of the pressure causes the mantle rock to become magma.
What plate boundary is decompression melting?Decompression melting commonly occurs at divergent plate boundaries, where two tectonic plates are moving away from each other. Mid-ocean ridges are the classic example, but adiabatic melting also occurs during continental lithospheric extension and in some mantle plumes.
How does decompression melting occur quizlet?How does decompression melting occur? -When hot, liquid mantle rock ascends, it moves to areas of lower pressure. This reduction in pressure allows the hot material to melt into a less viscous liquid phase.
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What is the process by which decompression melting produces magma at divergent plate boundaries?
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