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Temperature within the Earth increases with greater depth. Highly viscous or partially molten rock at temperatures between 650 to 1,200C (1,202 to 2,192F) is postulated to exist everywhere beneath the Earth's surface at depths of 50 to 60 miles (80 to 100 kilometers), and the temperature at the Earth's center, nearly 4,000miles (6,400km) deep, is estimated to be 5650 600 kelvins. The heat content of the earth is 1031 Joules. Much of the heat is believed to be created by decay of naturally radioactive elements. An estimated 45 to 90 percent of the heat escaping from the Earth originates from radioactive decay of elements within the mantle. Heat of impact and compression released during the original formation of the Earth by accretion of in-falling meteorites. Heat released as abundant heavy metals (iron, nickel, copper) descended to the Earth's core. Some heat may be created by electromagnetic effects of the magnetic fields involved in Earth's magnetic field. 10 to 25% of the heat flowing to the surface may be produced by a sustained nuclear fission reaction in Earth's inner core, the "georeactor" hypothesis. Heat may be generated by tidal force on the Earth as it rotates; since land cannot flow like water it compresses and distorts, generating heat. Present-day major heat-producing isotopes Heat release [W/kg isotope] Mean mantle concentration [kg isotope/kg mantle] Heat release [W/kg mantle] Sequence of the burning of a shrub by geothermal heat. Heat flows constantly from its sources within the Earth to the surface. Total heat loss from the earth is 42 TW (4.2 1013 Watts). This is approximately 1/10 watt/square meter on average, (about 1/10,000 of solar irradiation,) but is much more concentrated in areas where thermal energy is transported toward the crust by Mantle plumes; a form of convection consisting of upwellings of higher-temperature rock. These plumes can produce hotspots and flood basalts. The Earth's crust effectively acts as a thick insulating blanket which must be pierced by fluid conduits (of magma, water or other) in order to release the heat underneath. More of the heat in the Earth is lost through plate tectonics, by mantle upwelling associated with mid-ocean ridges. The final major mode of heat loss is by conduction through the lithosphere, the majority of which occurs in the oceans due to the crust there being much thinner than under the continents. The heat of the earth is replenished by radioactive decay at a rate of 30 TW. The global geothermal flow rates are more than twice the rate of human energy consumption from all primary sources. The geothermal gradient has been exploited for space heating and bathing since ancient roman times, and more recently for generating electricity. About 10 GW of geothermal electric capacity is installed around the world as of 2007, generating 0.3% of global electricity demand. An additional 28 GW of direct geothermal heating capacity is installed for district heating, space heating, spas, industrial processes, desalination and agricultural applications. The geothermal gradient varies with location and is typically measured by determining the bottom open-hole temperature after borehole drilling. To achieve accuracy the drilling fluid needs time to reach the ambient temperature. This is not always achievable for practical reasons. In stable tectonic areas in the tropics a temperature-depth plot will converge to the annual average surface temperature. However, in areas where deep permafrost developed during the Pleistocene a low temperature anomaly can be observed that persists down to several hundred metres. The Suwaki cold anomaly in Poland has led to the recognition that similar thermal disturbances related to Pleistocene-Holocene climatic changes are recorded in boreholes throughout Poland, as well as in Alaska, northern Canada, and Siberia. In areas of Holocene uplift and erosion (Fig. 1) the initial gradient will be higher than the average until it reaches an inflection point where it reaches the stabilized heat-flow regime. If the gradient of the stabilized regime is projected above the inflection point to its intersect with present-day annual average temperature, the height of this intersect above present-day surface level gives a measure of the extent of Holocene uplift and erosion. In areas of Holocene subsidence and deposition (Fig. 2) the initial gradient will be lower than the average until it reaches an inflection point where it joins the stabilized heat-flow regime. In deep boreholes, the temperature of the rock below the inflection point generally increases with depth at rates of the order of 20 K/km or more.[citation needed] Fourier's law of heat flow applied to the Earth gives q = Mg where q is the heat flux at a point on the Earth's surface, M the thermal conductivity of the rocks there, and g the measured geothermal gradient. A representative value for the thermal conductivity of granitic rocks is M = 3.0 W/mK. Hence, using the global average geothermal conducting gradient of 0.02 K/m we get that q = 0.06 W/m. This estimate, corroborated by thousands of observations of heat flow in boreholes all over the world, gives a global average of 6102 W/m. Thus, if the geothermal heat flow rising through an acre of granite terrain could be efficiently captured, it would light four 60 watt light bulbs. A variation in surface temperature induced by climate changes and the Milankovitch cycle can penetrate below the Earth's surface and produce an oscillation in the geothermal gradient with periods varying from daily to tens of thousands of years and an amplitude which decreases with depth and having a scale depth of several kilometers. Melt water from the polar ice caps flowing along ocean bottoms tends to maintain a constant geothermal gradient throughout the Earth's surface. If that rate of temperature change were constant, temperatures deep in the Earth would soon reach the point where all known rocks would melt. We know, however, that the Earth's mantle is solid because it transmits S-waves. The temperature gradient dramatically decreases with depth for two reasons. First, radioactive heat production is concentrated within the crust of the Earth, and particularly within the upper part of the crust, as concentrations of uranium, thorium, and potassium are highest there: these three elements are the main producers of radioactive heat within the Earth. Second, the mechanism of thermal transport changes from conduction, as within the rigid tectonic plates, to convection, in the portion of Earth's mantle that convects. Despite its solidity, most of the Earth's mantle behaves over long time-scales as a fluid, and heat is transported by advection, or material transport. Thus, the geothermal gradient within the bulk of Earth's mantle is of the order of 0.3 kelvin per kilometer, and is determined by the adiabatic gradient associated with mantle material (peridotite in the upper mantle). This heating up can be both beneficial or detrimental in terms of engineering: Geothermal energy can be used as a means for generating electricity, by using the heat of the surrounding layers of rock underground to heat water and then routing the steam from this process through a turbine connected to a generator. On the other hand, drill bits have to be cooled not only because of the friction created by the process of drilling itself but also because of the heat of the surrounding rock at great depth. Very deep mines, like some gold mines in South Africa, need the air inside to be cooled and circulated to allow miners to work at such great depth. a b Turcotte, D. L.; Schubert, G. (2002). "4". Geodynamics (2 ed.). Cambridge, England, UK: Cambridge University Press. pp.136137. ISBN 978-0-521-66624-4. Vlaar, N; Vankeken, P; Vandenberg, A (1994). "Cooling of the earth in the Archaean: Consequences of pressure-release melting in a hotter mantle". Earth and Planetary Science Letters 121: 1. doi:10.1016/0012-821X(94)90028-0. Alfe, D.; M. J. Gillan, G. D. Price (2003-02-01). "Thermodynamics from first principles: temperature and composition of the Earths core" (PDF). Mineralogical Magazine 67 (1): 113123. doi:10.1180/0026461026610089. Retrieved 2007-03- Magazine. Turcotte, D. L.; Schubert, G. (2002). "4". Geodynamics (2 ed.). Cambridge, England, UK: Cambridge University Press. pp.137. ISBN 978-0-521-66624-4. a b Sclater, John G; Parsons, Barry; Jaupart, Claude (1981). "Oceans and Continents: Similarities and Differences in the Mechanisms of Heat Loss". Journal of Geophysical Research 86: 11535. doi:10.1029/JB086iB12p11535. The Frozen Time, from the Polish Geological Institute a b Stacey, Frank D. (1977). Physics of the Earth (2nd ed.). New York: John Wiley & Sons. ISBN 0-471-81956-5. pp. 183-4 Sleep, Norman H.; Kazuya Fujita (1997). Principles of Geophysics. Blackwell Science. ISBN 0-86542-076-9. pp. 187-9 "Geothermal Resources". DOE/EIA-0603(95) Background Information and 1990 Baseline Data Initially Published in the Renewable Energy Annual 1995. Retrieved May 4, 2005. Geothermal power Geothermal electricity Geothermal heating Geothermal gradient Armenia Australia Canada Chile China Denmark El Salvador Germany Iceland Japan Kenya Lithuania Mexico New Zealand Portugal Philippines Romania Russia Turkey United Kingdom United States West Indies Aquaculture Desalination Geothermal heat pump District heating Binary Cycle EGS Heat pump Baseload power Capacity factor Energy storage Energy subsidies EROEI Portals: Energy Sustainable development Categories: Geological processes Geophysics Structure of the Earth Geothermal energyHidden categories: All articles with unsourced statements Articles with unsourced statements from June 2008 Pages containing cite templates with deprecated parameters The e-commerce company in China offers quality products such as China Other Application Software , China Ebook, and more. 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