APPLICATION - Charles Richter devised a logarithmic scale for measuring the magnitude m of an earthquake based on the energy release E in joules:\nm(e)=(2/3)log(e/10^4.4)\n\nFind the magnitude of a quake that as an energy release of , roughly the amount of energy released by the Clumbia quake in 1906. Write your answer in the space below rounded to the nearest 0.01\nenergy released= 2*10^17
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"The answer if four" -Rodney Dangerfield in "Back to School"
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The short answer is, you don't.\n\nThe log is the exponent you put on the base to get the number you want the log of.  base 10 log of 100 is 2, because 10^2=100.  But all powers of 1 are 1, and all powers of 0 are 0.
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go to\n\nhttp://earthquake.usgs.gov/\n\nits a great site - tell you when, where and how big
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An earthquake is a phenomenon that results from and is powered by the sudden release of stored energy in the crust that propagates seismic waves. At the Earth's surface, earthquakes may manifest themselves by a shaking or displacement of the ground and sometimes tsunamis, which may lead to loss of life and destruction of property.\n\nEarthquakes may occur naturally or as a result of human activities. In its most generic sense, the word earthquake is used to describe any seismic event—whether a natural phenomenon or an event caused by humans—that generates seismic waves.\n\nTypes of earthquakes\n\nNaturally occurring earthquakes :-\nMost naturally occurring earthquakes are related to the tectonic nature of the Earth. Such earthquakes are called tectonic earthquakes. The Earth's lithosphere is a patchwork of plates in slow but constant motion caused by the heat in the Earth's mantle and core. Plate boundaries grind past each other, creating frictional stress. When the frictional stress exceeds a critical value, called local strength, a sudden failure occurs. The boundary of tectonic plates along which failure occurs is called the fault plane. When the failure at the fault plane results in a violent displacement of the Earth's crust, the elastic strain energy is released and seismic waves are radiated, thus causing an earthquake. This processes of strain, stress, and failure is referred to as the Elastic-rebound theory. It is estimated that only 10 percent or less of an earthquake's total energy is radiated as seismic energy. Most of the earthquake's energy is used to power the earthquake fracture growth and is converted into heat. Therefore, earthquakes lower the Earth's available potential energy, though these losses are negligible\nEarthquakes occurring at boundaries of tectonic plates are called interplate earthquakes, while the less frequent events that occur in the interior of the lithospheric plates are called intraplate earthquakes.\n\nThe majority of tectonic earthquakes originate at depths not exceeding a few tens of kilometers. In subduction zones, where older and colder oceanic crust descends beneath another tectonic plate, earthquakes may occur at much greater depths (up to hundreds of kilometers). These seismically active areas of subduction are known as Wadati-Benioff zones. Deep focus earthquakes are another phenomenon associated with a subducting slab. These are earthquakes that occur at a depth at which the subducted lithosphere should no longer be brittle, due to the high temperature and pressure. A possible mechanism for the generation of deep focus earthquakes is faulting caused by olivine undergoing a phase transition into a spinel structure.\nEarthquakes may also occur in volcanic regions and are caused by the movement of magma in volcanoes. Such quakes can be an early warning of volcanic eruptions.\n\nA recently proposed theory suggests that some earthquakes may occur in a sort of earthquake storm, where one earthquake will trigger a series of earthquakes each triggered by the previous shifts on the fault lines, similar to aftershocks, but occurring years later, and with some of the later earthquakes as damaging as the early ones. Such a pattern was observed in the sequence of about a dozen earthquakes that struck the North Anatolian Fault in Turkey in the 20th Century, the half dozen large earthquakes in New Madrid in 1811-1812, and has been inferred for older anomalous clusters of large earthquakes in the Middle East and in the Mojave Desert.\n\n\nInduced earthquakes :- \n\nSome earthquakes have anthropogenic sources, such as extraction of minerals and fossil fuel from the Earth's crust, the removal or injection of fluids into the crust, reservoir-induced seismicity, massive explosions, and collapse of large buildings. Seismic events caused by human activity are referred to by the term induced seismicity. They however are not strictly earthquakes and usually show a dif
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(m)\n\nAustralian and American researchers investigating forces exerted on the Indo-Australian tectonic plate have discovered that the considerable stresses being exerted on the plate could be leading to its breaking up.\n\nARC Professorial Fellow, Mike Sandiford, from the University of Melbourne’s School of Earth Sciences was recently awarded ARC funding for research aimed at understanding the forces that drive the motion of the Earth’s tectonic plates and the distribution of stresses in the Earth’s crust that give rise to great earthquakes such as the magnitude 9 Boxing Day Sumatran quake.\n\nProfessor Sandiford says the research shows that as much as 10 per cent of the huge amounts of energy being created at plate connection points at Sumatra and Java are being transferred back into our plate and causing major stresses.\n\n“This is enough stress to contribute to mild earthquake activity in the central regions of the plate, such as in the Australian continent or central Indian Ocean, and provides us with clues as to why our plate has been slowly breaking up,” he says.\n\n“The Indian Ocean quakes are, in effect, leading to the active rupture of the Indo-Australian plate into separate Indian and Australian plates. This new research provides us with important information about the stresses that are driving this drawn out tectonic plate divorce.”\n\nThe research, which was conducted in collaboration with Wouter Pieter Schellart of the Australian National University and David Coblentz of the Los Alamos National Laboratory in the US, will be published in the journal Geology (27 January).\n\nThe research is also important for understanding why smaller intra-plate earthquakes such as the 1989 Newcastle quake, which occurred nowhere near the edge of the plate, take place. Up to now, why earthquakes occur in apparently safe zones in the centre of plates has not been very well understood.\n\nProfessor Sandiford says, “Earthquakes such as the 1989 Newcastle quake that killed 13 people and caused more than $1 billion in damages are just one manifestation of mild tectonic activity that has been affecting the Australian continent for the last 5-10 million years.”\n\nThe new research shows that stresses originating at points of collision between two plates are being dissipated back into our plate and generating enormous internal stresses.\n\nThe ARC funded project will map the spatial and temporal pattern of this tectonic activity and relate it to the factors that drive the motion of the Indo-Australian plate.\n\n“This research will contribute to our understanding of the factors that drive plate motion, to earthquake risk assessment in Australia and other comparatively stable continental regions, and to the factors that have shaped our distinctive Australian landscapes,” he says.\n\nBACKGROUND INFORMATION\n\nWhat causes tectonic plates to move?\nThe Earth is made up of a series of layers. The outermost layer is called the crust and the innermost is the core. In between lies an area called the mantle (in turn made up of upper and lower mantle), which is arguably the most important when it comes to understanding where big earthquakes occur.\n\nThe outer part of the Earth, comprising the crust and top 100 or so kilometres of the mantle (together called the lithosphere), consists of a collection of eight major plates which almost fit perfectly together. The continents and oceans all lie on these plates, the major ones referred to as the African, Eurasian, Indo-Australian, Antarctic, Philippine, Pacific, Nazca, North American and South American, depending on their geographic location.\n\nThese plates (also referred to as tectonic plates) float on the softer mantle underneath. Convection currents within the upper mantle layer are a major driving force driving plate motion and therefore behind earthquake activity.\n\nThe lower sections of the mantle closest to the molten core of the earth are also the hottest parts of this la
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Well, if you convert grams to kilograms, then you have\n\ne [=] kg*(m^2/s^2) [=] kg*(m/s^2)*m [=] N*m [=] J\n\nHowever, the units of E are determined by the units of mass, distance, and time that you use, and consequently could by in any of the units of energy.\n\nI'm not sure what english units you mean, but                               1 J = .73 feet*pound_force.\n\nFor unit conversions, consider using google or download a more comprehensive freeware unit converter, like Uconeer. I use Uconeer for the more obscure unit transformations, and tabulated values for more common conversions.  Google it.
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Earthquakes 10.5 are impossibly big.  Places in America where you get earthquakes as big as 9 only happen along the coast of Alaska.  The biggest earthquake that can happen on the San Andreas is about 8.  Volcanoes in the US are only related to some faults, not all, and they are not interconnected, so one eruption is not related to nor does it cause another.\n\nHere are some basics on earthquakes/volcanism to help you with why this is physically impossible:\n\nEarthquakes: \nIt all comes down to stress and strain from the interaction of different plates, chiefly at the boundaries. It is not 'the plates rubbing together' as many people say; or at least that's a very simplistic view.\n\nPlate tectonics causes stress on the continents and oceans, all over the surface of the earth. In some places, the stress is very small (usually within the plates). Elsewhere, the stress is high, usually where the plates meet each other. Since each plate moves, when two come in contact, the stress each other. They can push on each other and cause compressional stress, they can pull with extensional stress, and they can slide past or shear each other with tensional stress.\n\nFaulting, causing earthquakes, comes from the fact that this stress is building up all the time, but rocks and continents are strong materials. Just like hitting a rock with a small hammer, you do put stress on it, but a small amount. It would take a sledgehammer to put enough strain (effects and accumulation of stress) to build up and cause breakage. In the earth, the area around an active fault builds up strain from the stress of plate tectonics. Most faults become locked, because of this strength, and thus can not release their strain. Away from the fault, the stress produces very small and slow movement of the rock masses as a whole. Eventually, the strain is too much and the rest of the plate has moved too far and the fault releases the strain build-up all at once in a big stress release called an earthquake. This is called the elastic rebound theory, and it explains most (but not all) movements.\n\nThis is why an earthquake's size is relative to the fault size. The bigger the fault, the bigger the strain build up, and the bigger the release in an earthquake. Subduction zones and collision zones, where large portions of plates actually can rub together as a whole, have the really big earthquakes, like the 2004 Sumatra earthquake. In other plate boundaries, the entire plate boundary does not act together, so the faults become spread out and many faults take up the strain from the tectonic stress, like with the San Andreas Fault in California (it only takes up ~3/4 of the stress between the plates).\n\nEarthquakes are really tricky things; there is still so much we need to learn. As of now, there is no way to predict them, but we can say where the danger is highest and about how long between events.\n\nVolcanoes:\nThere are several processes in Plate Tectonics that cause volcanism, but they result in two main types of volcanism.\n\nVolcanism in subduction is caused by volitals, like H2O, CO2. These are carried down by the plate, mainly in the form of weak minerals. These minerals break down with pressure and temperature into stronger minerals that don't contain water and carbon dioxide. The leftover gases and liquids travel into the mantle (the mantle wedge) and hydrate the mantle, causing melting. The melt rises and then... volcano!\n\nThe other main cause is from rising mantle material, which forms decompression melting. Basically, hot mantle is kept from melting by the pressure of the earth at depth. When this material rises, the pressure drops much faster than the temperature, and thus it partially melts. This mainly occurs at divergent boundaries and hot spots, which are areas in plate tectonics that have rising materials or spreading.
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E = mc^2 = 1kg * (3*10^8)^2 = 9^10^16 Joules
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I can't find what you are looking for - it appears your book is likely out of print. However, there is a new novel baed during the 1906 earthquake called 1906: A Novel by James Dalessandro that was just published. I hope that helps.\n\nGood luck!
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The way I see it.... u calculate its impulse with the ground.... mass1*velocity1 (pre-shock)=m2*v2 (after shock) then caculate it's potential energy by newton's law of gravity using v2....(god I'm being a GEEK!)
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Well the energy is equal to planck's constant times the frequency, so that would be 6.62 x 10^-34 times the frequency which would be 5.96 x 10^14 Hz, so your answer is 3.95 x 10^-19 Joules
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- 217: lightning damage, but was restored\n- 442: earthquake, massive damage\n- 508: earthquake, massive damage\n- 847: earthquake, massive damage\n- 1349: earthquake, massive damage\n- Renaissance period (1400-1600 c.e.): marble was taken to aid the building of St. Peter's Basilica and other buildings
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It is generally said that the law of conservation of mass holds for ordinary chemical reactions, and for all intensive purposes, it does.\nHowever, technically, there is a VERY small change in the mass (too small to even matter to most things) when energy is given off or gained.\n\nIn the case of 56 kJ being released when 1 g of natural gas combusts, there is an associated change in mass of only 6.2 E-13 kg (6.2 E -10 grams).\nE = mc^2\n56000 Joules = m (3 E8)^3\nm = 56000 / (9 E16)\nThis is such a small number, it is very easy to ignore it as it would be near impossible to measure such a small amount anyway.
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THE NEWCASTLE EARTHQUAKE\nOn December 28, 1989, a magnitude 5.6 earthquake struck Newcastle, causing extensive damage and killing 13 people. This earthquake proved that even Australia is not immune from damaging earthquakes causing significant human and economic loss.\n\nMost of the damage occured to unreinforced masonry buildings which had been built between 1900 and 1950. Over 3000 residences were damaged throughout the city. Until recently Newcastle was a steel manufacturing city, (BHP Steel closed late 1999) but at the time of the earthquake the steel mills were not severly damaged and gas and electricity sub stations did not incur major damage.\n\nGenerally speaking, most modern structures were generally not damaged; the exception was the Newcastle Workers Club, where a section built in 1972 collapsed, killing 10 people. The club was built in two main parts; an older unreinforced masonry section and a newer concrete frame section four stories high with underground parking. The collapse of the Newcastle Workers Club began at the top of the club causing the building to cascade into itself trapping patrons and workers within the building.
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Here is the USGS list of historic earthquakes. It does include many (probably too many) events since 1980. There are links on the page that will lead to you lists sorted by region, magnitude, etc.:\nhttp://earthquake.usgs.gov/regional/world/historical.php\n\nHere is the list of volcanic eruptions that have had more than 300 casualties. It is a little harder to sort out the most significant volcanic eruptions since we have no scale for comparing them.\nhttp://volcanoes.usgs.gov/Hazards/Effects/Fatalities.html\n\nCORRECTION: THERE IS A SCALE FOR VOLCANIC ERUPTIONS, BUT THOSE ARE NOT CLASSIFIED USING THE VEI SCALE:\nhttp://lvo.wr.usgs.gov/sizes.html\n\nThis site at the Smithsonian Global Volcanism Program is searchable by year, and has links to each significant eruption:\nhttp://www.volcano.si.edu/world/find_eruptions.cfm\n\nI haven't seen this but thought this CD from the Smithsonian looked interesting. It has a global dataset of volcanic eruptions and earthquakes since 1960 (but costs $20).\nhttp://www.volcano.si.edu/info/products/eqerupt/eqerupt.cfm\n\nHere is the USGS list of Historical Landslides starting in 1958 and continuing to date:\nhttp://landslides.usgs.gov/learningeducation/historical.php\n\nHere is a list of major Pacific tsunamis from 1981 to 1997 at the Russian Academy of Science. :\nhttp://omzg.sscc.ru/tsulab/recent.html\nThe site has quite a few other lists of tsunami events grouped by ocean basin.\nhttp://omzg.sscc.ru/tsulab/\n\n\nAnother type of geologic event that is hard to pinpoint because it is a gradual process is subsidence. This is an informative website that lists various types of subsidence and where it is happening:\nhttp://www.earthsci.org/processes/struct/subside/Subsidence.htm
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There are other scales but the Richter scale is used almost exclusively.  Read this article at Wikipedia for more information, http://en.wikipedia.org/wiki/Richter_scale
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Conserve both momentum and total energy (i.e., potential energy plus kinetic energy).\n\nMy coordinate system will have the pendulum lifted to the left and the block on the right moving left, so that the initial momentum is - M2 Vo2.\n\nIt will also have the block at height 0, so the initial potential is M1 g h where h is the initial height of the pendulum, which looks like L(1 - sin(10 degrees)).\n\nThe initial kinetic energy is of course (1/2) M2 (Vo2)^2.\n\nSo ...\n\ninitial momentum: - M2 Vo2\ninitial energy: M1 g h + (1/2) M2 (Vo2)^2\n\nAfter the collision the potential energy has decreased to zero, and if w is the combined velocity of the two masses then ...\n\nfinal momentum: (M1 + M2)w\nfinal energy: (1/2)(M1 + M2)w^2 + [the energy "loss" from the slight heating and deformation of the two masses sticking].