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Part I. Mt. St. Helens

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Part I. Mt. St. Helens The Geology of Pacific Northwest Volcanoes, Mountains and Earthquakes Lab 3: Cascade Volcanoes Name: ___________________________________________________ Date: ____________________ This contains material adapted from Richard Abbot (Appalachian State University, Department of Geology) and from the USGS Volcanoes! 1997 Teacher packet. Part I. Mt. St. Helens In the illustration at the right is a vertical cross‐ section (from A to A’) of Earth’s crust and mantle from west of the Cascadia subduction zone to east of Mt. St. Helens and a map showing this region and the location of the vertical cross‐section. 1. What is the distance between the Volcano and the Cascadia subduction zone fault? ___________ 2. What is the depth of the Juan de Fuca plate beneath Mt. St. Helens? _________ The cross‐section (above the map) show the relations between the convergent plate boundary and volcanism. In the case of Mount St. Helens, like the other stratovolcanoes of the Cascades, the production of the andesitic/rhyolitic magma is ultimately related to the subduction of the Juan de Fuca plate beneath the western edge of the North America plate. Oceanic crust of the Juan de Fuca plate and sedimentary material are being shoved downward, toward the east, underneath North America. This down‐going material undergoes metamorphism as it becomes exposed to progressively higher pressures and temperatures in the interior of the earth beneath North America. Temperatures at depths of the top of the Juan de Fuca plate directly below Mt. St. Helens can be as high as 1,200° C, hot enough to cause some partial melting of the metamorphosed basalt of the subducting oceanic crust. The metamorphism also releases volatile (gas) components such as H2O, CO2, and SO2. The relatively small amounts of basaltic magma and rather large amounts of volatile gasses migrate upward, ultimately encountering the base of the overlying continental crust. Here, the basaltic magma and volatile gasses contribute to partial melting of the base of the continental crust. The magma thus formed is andesitic and rhyolitic, reflecting the composition of the lower part of the continental crust. Generally, only very small amounts of the basaltic magma ever reach the surface. The greater part of the basaltic magma becomes mixed, sort of homogenized, with the andesitic/rhyolitic magma. This andesitic/rhyolitic magma readily dissolves, quite literally soaks up, the volatile components. Under the very high pressures at such depths near the base of the continental crust these dissolved gasses are effectively trapped in the magma. However, the buoyant, gas‐charged magma tends to work its way upward toward the surface (intrusion). Most of the andesitic/rhyolitic magma cools and crystallizes before it ever reaches 1 | Page The Geology of Pacific Northwest Volcanoes, Mountains and Earthquakes Lab 3: Cascade Volcanoes the surface, forming sometimes vast plutonic (intrusive) bodies of granodiorite/granite. Only comparatively small amounts of the gas‐charged andesitic/rhyolitic magma ever reach the surface, but when this happens ‐ LOOK OUT! The rapid formation of gas bubbles in the magma and their explosive expansion can have catastrophic effects. 3. Stratovolcanoes are typically circular in map view. The radius of Mount St. Helens is about 6 km at the base, and the elevation of the base is about 1 km above sea level. Before the eruption of May, 1980, the elevation at the top of Mount St. Helens was about 3 km. Using this information, and modeling the stratovolcano as a simple cone‐shape, estimate the volume of volcanic material in Mount St. Helens, in cubic kilometers (km3). To remind you, the volume of a cone is given by the following formula, Volume = (1/3)*pi*r2*h, where pi = ~ 3.14, r = radius of the cone, and h = height of the cone. Volume = _________________ The next questions refer to these maps of Mt. St. Helens from before and from after the eruption. This map is adapted by the USGS from Brugman and Post, 1981 http://pubs.er.usgs.gov/publication/cir850D 2 | Page The Geology of Pacific Northwest Volcanoes, Mountains and Earthquakes Lab 3: Cascade Volcanoes 4. What is the slope and angle of the slope of the surface of Mount St. Helens along the thick black line in the "before" map above? The length of the thick black line is 2,000 m. Recall that slope = rise/run. Convert this from a fraction to a percent: 5. Shield Volcanoes have slopes that range from 9 % along their lower slopes to 18 % along their higher slopes. How does the slope you calculated in step 3 compare with shield volcanoes? 6. Why are these slopes different? 7. One way to examine the effects of the eruption is to construct "before" and "after" topographic profiles of the volcano. a. Construct “before” and “after” topographic profiles on the grids that are placed along the A‐A’ profile lines. The elevation contours are in meters. b. On your copy of the post‐eruption profile use colored pencils to denote the following regions, (1) where there has been no change, (2) where material has been removed, and (3) where material has been added (deposited). Create a legend here that lists what color you used for each of the three regions: 3 | Page The Geology of Pacific Northwest Volcanoes, Mountains and Earthquakes Lab 3: Cascade Volcanoes 8. The amount of material (6.5 km3) that was removed from Mount St. Helens represents what percentage of the original volcano? 9. What is the vertical exaggeration of your profiles? Part II. The Age of a volcanic deposit Have you ever looked at a tree stump and noticed its rings? Count the rings and you will know how old the tree is. Each ring represents 1 year in the life of the tree. If you look closely at tree rings, however, you will see that the spaces between rings vary in width. Trees do not grow the same amount each year. You can “read” these tree rings and find out what year there was an eruption of Mount Katmai in Alaska. What you know: 1. This tree was growing 48 kilometers (29 miles) northwest of Katmai Volcano. 2. After the eruption, the forests were blanketed in ash. 3. This tree’s growth decreased for some years after the eruption, but then it increased. 4. This tree was cut down in 1962. What you want to find out: 1. The tree’s age: (Count the number of rings from the center of the tree to the bark. Each dark band represents 10 years.) __________________ 2. The year the tree started to grow: a. (the year the tree was cut) ‐ (the age of the tree) = (the year the tree started to grow) b. _________ ‐ _________ = ____________ 3. The year of the eruption: (Count the number of rings from the center to the first thin ring.) ______________ 4. The number of years the tree’s growth decreased: (Count the number of thin tree rings) ______________ 5. The number of years the tree’s growth increased: (Count the number of wide rings.) ______________ 6. Why do you think the tree’s growth increased? 4 | Page The Geology of Pacific Northwest Volcanoes, Mountains and Earthquakes Lab 3: Cascade Volcanoes Part III. Recurrence of Cascades Volcanic Eruptions Volcanic eruptions pose a number of hazards that put people and their belongings at risk. Part of evaluating these hazards includes making estimates of the likelihood of an eruption. Many are familiar with the concept of whether a volcano is active or if it is dormant. Many volcanologists in the USA and internationally consider a volcano to be active if it has erupted in the last 10,000 years. Likewise, if a volcano has not erupted in the last 10 ka, we consider it dormant. Below is a plot showing the eruptions of the major Cascade volcanoes over the past 4 ka. In order to evaluate the relative hazards that each of these volcanoes may pose to people, we would like to make an estimate of the recurrence of their eruptions. We will do this by finding the average time between eruptions. 1. Calculate the mean RI for these Cascade volcanoes. Step 1. Determine the number of eruptions for each volcano. Also, estimate the years ago of the last eruption Step 2. Calculate the Recurrence Interval (RI) for each Cascades volcano by dividing the number of inter‐ eruption times (the number of eruptions minus one) by the time span (4 ka). List these values below: 5 | Page The Geology of Pacific Northwest Volcanoes, Mountains and Earthquakes Lab 3: Cascade Volcanoes Volcano Years Ago of Number of Math Recurrence Ratio Last Eruption Eruptions Interval (RI) Mount Baker: _______ __________ ___________________ __________ _____ Glacier Peak: _______ __________ ___________________ __________ _____ Mount Rainer: _______ __________ ___________________ __________ _____ Mount St. Helens: _______ __________ ___________________ __________ _____ Mount Adams: _______ __________ ___________________ __________ _____ Mount Hood: _______ __________ ___________________ __________ _____ Mount Jefferson: _______ __________ ___________________ __________ _____ Three Sisters: _______ __________ ___________________ __________ _____ Newberry Volcano: _______ __________ ___________________ __________ _____ Crater Lake: _______ __________ ___________________ __________ _____ Medicine Lake Volcano: _______ __________ ___________________ __________ _____ Mount Shasta: _______ __________ ___________________ __________ _____ Lassen Peak: _______ __________ ___________________ __________ _____ 2. One general way to evaluate how likely a volcano might erupt is to compare the RI with the timing of the last eruption. For example, let’s consider two volcanoes. Volcano A: the RI = 500 years and it has been 1,000 years since the last eruption. Volcano B: the RI = 500 years and it has been 100 years since the last eruption. Volcano A is probably closer to having an eruption sooner than volcano B.
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