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Structure of the Earth
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Structure of the Earth
The internal structure of the Earth is layered in spherical shells: an outer silicate solid crust, a highly viscous asthenosphere and mantle, a liquid outer core that is much less viscous than the mantle, and a solid inner core. Scientific understanding of the internal structure of the Earth is based on observations of topography and bathymetry, observations of rock in outcrop, samples brought to the surface from greater depths by volcanoes or volcanic activity, analysis of the seismic waves that pass through the Earth, measurements of the gravitational and magnetic fields of the Earth, and experiments with crystalline solids at pressures and temperatures characteristic of the Earth's deep interior.
Contents
1 Mass
2 Structure
2.1 Crust
2.2 Mantle
2.3 Core
3 See also
4 References
5 Further reading
6 External links
Mass[edit]
The force exerted by Earth's gravity can be used to calculate its mass. Astronomers can also calculate Earth's mass by observing the motion of orbiting satellites. Earth’s average density can be determined through gravimetric experiments, which have historically involved pendulums.
The mass of Earth is about 7024600000000000000♠6×1024 kg.[1]
Structure[edit]
Earth's radial density distribution according to the preliminary reference earth model (PREM).[2]
Earth's gravity according to the preliminary reference earth model (PREM).[2] Comparison to approximations using constant and linear density for Earth's interior.
Mapping the interior of Earth with earthquake waves.
Schematic view of the interior of Earth. 1. continental crust – 2. oceanic crust – 3. upper mantle – 4. lower mantle – 5. outer core – 6. inner core – A: Mohorovičić discontinuity – B: Gutenberg Discontinuity – C: Lehmann–Bullen discontinuity.
The structure of Earth can be defined in two ways: by mechanical properties such as rheology, or chemically. Mechanically, it can be divided into lithosphere, asthenosphere, mesospheric mantle, outer core, and the inner core. Chemically, Earth can be divided into the crust, upper mantle, lower mantle, outer core, and inner core. The geologic component layers of Earth[3][not in citation given] are at the following depths below the surface:
Depth
Layer
Kilometres
Miles
0–60 0–37 Lithosphere (locally varies between 5 and 200 km)
0–35 0–22 … Crust (locally varies between 5 and 70 km)
35–60 22–37 … Uppermost part of mantle
35–2,890 22–1,790 Mantle
210-270 130-168 … Upper mesosphere (upper mantle)
660–2,890 410–1,790 … Lower mesosphere (lower mantle)
2,890–5,150 1,790–3,160 Outer core
5,150–6,360 3,160–3,954 Inner core
The layering of Earth has been inferred indirectly using the time of travel of refracted and reflected seismic waves created by earthquakes. The core does not allow shear waves to pass through it, while the speed of travel (seismic velocity) is different in other layers. The changes in seismic velocity between different layers causes refraction owing to Snell's law, like light bending as it passes through a prism. Likewise, reflections are caused by a large increase in seismic velocity and are similar to light reflecting from a mirror.
Crust[edit]
Main article: Crust (geology)
The crust ranges from 5–70 kilometres (3.1–43.5 mi) in depth and is the outermost layer. The thin parts are the oceanic crust, which underlie the ocean basins (5–10 km) and are composed of dense (mafic) iron magnesium silicate igneous rocks, like basalt. The thicker crust is continental crust, which is less dense and composed of (felsic) sodium potassium aluminium silicate rocks, like granite. The rocks of the crust fall into two major categories – sial and sima (Suess,1831–1914). It is estimated that sima starts about 11 km below the Conrad discontinuity (a second order discontinuity). The uppermost mantle together with the crust constitutes the lithosphere. The crust-mantle boundary occurs as two physically different events. First, there is a discontinuity in the seismic velocity, which is most commonly known as the Mohorovičić discontinuity or Moho. The cause of the Moho is thought to be a change in rock composition from rocks containing plagioclase feldspar (above) to rocks that contain no feldspars (below). Second, in oceanic crust, there is a chemical discontinuity between ultramafic cumulates and tectonized harzburgites, which has been observed from deep parts of the oceanic crust that have been obducted onto the continental crust and preserved as ophiolite sequences.
Many rocks now making up Earth's crust formed less than 100 million (1×108) years ago; however, the oldest known mineral grains are about 4.4 billion (4.4×109) years old, indicating that Earth has had a solid crust for at least 4.4 billion years.[4]
Mantle[edit]
World map showing the position of the Moho.
Main article: Mantle (geology)
Earth's mantle extends to a depth of 2,890 km, making it the thickest layer of Earth. The mantle is divided into upper and lower mantle. The upper and lower mantle are separated by the transition zone. The lowest part of the mantle next to the core-mantle boundary is known as the D″ (pronounced dee-double-prime[5]) layer. The pressure at the bottom of the mantle is ≈140 GPa (1.4 Matm). The mantle is composed of silicate rocks that are rich in iron and magnesium relative to the overlying crust. Although solid, the high temperatures within the mantle cause the silicate material to be sufficiently ductile that it can flow on very long timescales. Convection of the mantle is expressed at the surface through the motions of tectonic plates. As there is intense and increasing pressure as one travels deeper into the mantle, the lower part of the mantle flows less easily than does the upper mantle (chemical changes within the mantle may also be important). The viscosity of the mantle ranges between 1021 and 1024 Pa·s, depending on depth.[6] In comparison, the viscosity of water is approximately 10−3 Pa·s and that of pitch is 107 Pa·s. The source of heat that drives plate tectonics is the primordial heat left over from the planet’s formation as well as the radioactive decay of uranium, thorium, and potassium in Earth’s crust and mantle.[7]
Core[edit]
Main articles: inner core and outer core
The average density of Earth is 7000551499999999999♠5.515 g/cm3.[8] Because the average density of surface material is only around 7000300000000000000♠3.0 g/cm3, we must conclude that denser materials exist within Earth's core. This result has been known since the Schiehallion experiment, performed in the 1770s. Charles Hutton in his 1778 report concluded that the mean density of the Earth must be about 9 5 {\displaystyle {\tfrac {9}{5}}} that of surface rock, concluding that the interior of the Earth must be metallic. Hutton estimated this metallic portion to occupy some 65% of the diameter of the Earth.[9] Hutton's estimate on the mean density of the Earth was still about 20% too low, at 7000450000000000000♠4.5 g/cm3 Henry Cavendish in his torsion balance experiment of 1798 found a value of 7000545000000000000♠5.45 g/cm3, within 1% of the modern value.[10] Seismic measurements show that the core is divided into two parts, a "solid" inner core with a radius of ≈1,220 km[11] and a liquid outer core extending beyond it to a radius of ≈3,400 km. The densities are between 9,900 and 12,200 kg/m3 in the outer core and 12,600–13,000 kg/m3 in the inner core.[12]
The inner core was discovered in 1936 by Inge Lehmann and is generally believed to be composed primarily of iron and some nickel. Since this layer is able to transmit shear waves (transverse seismic waves), it must be solid. Experimental evidence has at times been critical of crystal models of the core.[13] Other experimental studies show a discrepancy under high pressure: diamond anvil (static) studies at core pressures yield melting temperatures that are approximately 2000 K below those from shock laser (dynamic) studies.[14][15] The laser studies create plasma,[16] and the results are suggestive that constraining inner core conditions will depend on whether the inner core is a solid or is a plasma with the density of a solid. This is an area of active research.
In early stages of Earth's formation about 4.6 billion years ago, melting would have caused denser substances to sink toward the center in a process called planetary differentiation (see also the iron catastrophe), while less-dense materials would have migrated to the crust. The core is thus believed to largely be composed of iron (80%), along with nickel and one or more light elements, whereas other dense elements, such as lead and uranium, either are too rare to be significant or tend to bind to lighter elements and thus remain in the crust (see felsic materials). Some have argued that the inner core may be in the form of a single iron crystal.[17][18]
Under laboratory conditions a sample of iron–nickel alloy was subjected to the corelike pressures by gripping it in a vise between 2 diamond tips (diamond anvil cell), and then heating to approximately 4000 K. The sample was observed with x-rays, and strongly supported the theory that Earth's inner core was made of giant crystals running north to south.[19][20]
The liquid outer core surrounds the inner core and is believed to be composed of iron mixed with nickel and trace amounts of lighter elements.
Recent speculation suggests that the innermost part of the core is enriched in gold, platinum and other siderophile elements.[21]
The matter that comprises Earth is connected in fundamental ways to matter of certain chondrite meteorites, and to matter of outer portion of the Sun.[22][23] There is good reason to believe that Earth is, in the main, like a chondrite meteorite. Beginning as early as 1940, scientists, including Francis Birch, built geophysics upon the premise that Earth is like ordinary chondrites, the most common type of meteorite observed impacting Earth, while totally ignoring another, albeit less abundant type, called enstatite chondrites. The principal difference between the two meteorite types is that enstatite chondrites formed under circumstances of extremely limited available oxygen, leading to certain normally oxyphile elements existing either partially or wholly in the alloy portion that corresponds to the core of Earth.
Dynamo theory suggests that convection in the outer core, combined with the Coriolis effect, gives rise to Earth's magnetic field. The solid inner core is too hot to hold a permanent magnetic field (see Curie temperature) but probably acts to stabilize the magnetic field generated by the liquid outer core. The average magnetic field strength in Earth's outer core is estimated to be 25 Gauss (2.5 mT), 50 times stronger than the magnetic field at the surface.[24][25]
Recent evidence has suggested that the inner core of Earth may rotate slightly faster than the rest of the planet;[26] however, more recent studies in 2011[which?] found this hypothesis to be inconclusive. Options remain for the core which may be oscillatory in nature or a chaotic system.[citation needed] In August 2005 a team of geophysicists announced in the journal Science that, according to their estimates, Earth's inner core rotates approximately 0.3 to 0.5 degrees per year faster relative to the rotation of the surface.[27][28]
The current scientific explanation for Earth's temperature gradient is a combination of heat left over from the planet's initial formation, decay of radioactive elements, and freezing of the inner core.
See also[edit]
Earth sciences portal
Geological history of Earth
Lehmann discontinuity
Rain-out model
Travel to the Earth's center
References[edit]
Jump up ^ "2016 Selected Astronomical Constants" in The Astronomical Almanac Online, USNO–UKHO, ME = 5·9722×1024 kg ± 6×1020 kg
^ Jump up to: a b A. M. Dziewonski, D. L. Anderson (1981). "Preliminary reference Earth model" (PDF). Physics of the Earth and Planetary Interiors. 25 (4): 297–356. Bibcode:1981PEPI...25..297D. doi:10.1016/0031-9201(81)90046-7. ISSN 0031-9201.
Jump up ^ T. H. Jordan (1979). "Structural Geology of the Earth's Interior" (PDF). Proceedings of the National Academy of Sciences. 76 (9): 4192–4200. Bibcode:1979PNAS...76.4192J. doi:10.1073/pnas.76.9.4192. PMC 411539  . PMID 16592703.
Jump up ^ Breaking News | Oldest rock shows Earth was a hospitable young planet. Spaceflight Now (2001-01-14). Retrieved on 2012-01-27.
Jump up ^ Krieger, Kim (24 March 2004). "D Layer Demystified". Science News. American Association for the Advancement of Science. Retrieved 5 November 2016.
Jump up ^ Uwe Walzer, Roland Hendel, John Baumgardner Mantle Viscosity and the Thickness of the Convective Downwellings.
Jump up ^ Lawrence Berkeley National Laboratory (Berkeley Lab) is a Department of Energy (DOE) Office of Science lab managed by University of California., What Keeps the Earth Cooking? News Release by Paul Preuss, July 17, 2011
Jump up ^ "Planetary Fact Sheet". Lunar and Planetary Science. NASA. Retrieved 2 January 2009.
Jump up ^ Hutton, C. (1778). "An Account of the Calculations Made from the Survey and Measures Taken at Schehallien". Philosophical Transactions of the Royal Society. 68 (0). doi:10.1098/rstl.1778.0034.
Jump up ^ Tretkoff, Ernie (June 2008). "June 1798: Cavendish Weighs the World". APS News. 17 (6). American Physical Society. Retrieved 5 June 2018.
Jump up ^ Monnereau, Marc; Calvet, Marie; Margerin, Ludovic; Souriau, Annie (May 21, 2010). "Lopsided Growth of Earth's Inner Core". Science. 328 (5981): 1014–1017. Bibcode:2010Sci...328.1014M. doi:10.1126/science.1186212. PMID 20395477.
Jump up ^ Hazlett, James S.; Monroe, Reed; Wicander, Richard (2006). Physical geology : exploring the earth (6. ed.). Belmont: Thomson. p. 346. ISBN 9780495011484.
Jump up ^ Stixrude, Lars; Cohen, R.E. (January 15, 1995). "Constraints on the crystalline structure of the inner core: Mechanical instability of BCC iron at high pressure". Geophysical Research Letters. 22 (2): 125–128. Bibcode:1995GeoRL..22..125S. doi:10.1029/94GL02742.
Jump up ^ Benuzzi-Mounaix, A.; Koenig, M.; Ravasio, A.; Vinci, T. (2006). "Laser-driven shock waves for the study of extreme matter states". Plasma Physics and Controlled Fusion. 48 (12B). Bibcode:2006PPCF...48B.347B. doi:10.1088/0741-3335/48/12B/S32.
Jump up ^ Remington, Bruce A.; Drake, R. Paul; Ryutov, Dmitri D. (2006). "Experimental astrophysics with high power lasers and Z pinches". Reviews of Modern Physics. 78. Bibcode:2006RvMP...78..755R. doi:10.1103/RevModPhys.78.755.
Jump up ^ Benuzzi-Mounaix, A.; Koenig, M.; Husar, G.; Faral, B. (June 2002). "Absolute equation of state measurements of iron using laser driven shocks". Physics of Plasmas. 9 (6). Bibcode:2002PhPl....9.2466B. doi:10.1063/1.1478557.
Jump up ^ Cohen, Ronald; Stixrude, Lars. "Crystal at the Center of the Earth". Archived from the original on 2007-02-05. Retrieved 2007-02-05.
Jump up ^ Stixrude, L.; Cohen, R. E. (1995). "High-Pressure Elasticity of Iron and Anisotropy of Earth's Inner Core". Science. 267 (5206): 1972–5. Bibcode:1995Sci...267.1972S. doi:10.1126/science.267.5206.1972. PMID 17770110.
Jump up ^ BBC News, "What is at the centre of the Earth?. Bbc.co.uk (2011-08-31). Retrieved on 2012-01-27.
Jump up ^ Ozawa, H.; al., et (2011). "Phase Transition of FeO and Stratification in Earth's Outer Core". Science. 334 (6057): 792–794. Bibcode:2011Sci...334..792O. doi:10.1126/science.1208265.
Jump up ^ Wootton, Anne (2006). "Earth's Inner Fort Knox". Discover. 27 (9): 18.
Jump up ^ Herndon, J. M. (1980). "The chemical composition of the interior shells of the Earth". Proc. R. Soc. Lond. A372 (1748): 149–154. JSTOR 2398362.
Jump up ^ Herndon, J. M. (2005). "Scientific basis of knowledge on Earth's composition" (PDF). Current Science. 88 (7): 1034–1037.
Jump up ^ First Measurement Of Magnetic Field Inside Earth's Core. Science20.com. Retrieved on 2012-01-27.
Jump up ^ Buffett, Bruce A. (2010). "Tidal dissipation and the strength of the Earth's internal magnetic field". Nature. 468 (7326): 952–4. Bibcode:2010Natur.468..952B. doi:10.1038/nature09643. PMID 21164483.
Jump up ^ Chang, Kenneth (2005-08-25). "Earth's Core Spins Faster Than the Rest of the Planet". The New York Times. Retrieved 2010-05-24.
Jump up ^ Kerr, R. A. (2005). "Earth's Inner Core Is Running a Tad Faster Than the Rest of the Planet". Science. 309 (5739): 1313a. doi:10.1126/science.309.5739.1313a. PMID 16123276.
Jump up ^ Chang, Kenneth (26 August 2005) "Scientists Say Earth's Center Rotates Faster Than Surface" The New York Times Sec. A, Col. 1, p. 13.
Further reading[edit]
Drollette, Daniel (October 1996). "A Spinning Crystal Ball". Scientific American. 275 (4): 28–33.
Kruglinski, Susan (June 2007). "Journey to the Center of the Earth". Discover. Retrieved 9 July 2016.
Lehmann, I (1936). "Inner Earth". Bur. Cent. Seismol. Int. 14: 3–31.
Wegener, Alfred (1966). The origin of continents and oceans. New York: Dover Publications. ISBN 9780486617084.
External links[edit]
The Wikibook Historical Geology has a page on the topic of: Structure of the Earth
Media related to Structure of the Earth at Wikimedia Commons
Down To The Earth's Core (HD) on YouTube
The Earth's Core on In Our Time at the BBC
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Viral envelope
From Wikipedia, the free encyclopedia
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Schematic of a Cytomegalovirus
Some viruses (e.g. HIV and many animal viruses) have viral envelopes covering their protective protein capsids.[1] The envelopes are typically derived from portions of the host cell membranes (phospholipids and proteins), but include some viral glycoproteins. They may help viruses avoid the host immune system. Glycoproteins on the surface of the envelope serve to identify and bind to receptor sites on the host's membrane. The viral envelope then fuses with the host's membrane, allowing the capsid and viral genome to enter and infect the host.
The cell from which the virus itself buds will often die or be weakened and shed more viral particles for an extended period. The lipid bilayer envelope of these viruses is relatively sensitive to desiccation, heat, and detergents, therefore these viruses are easier to sterilize than non-enveloped viruses, have limited survival outside host environments, and typically must transfer directly from host to host. Enveloped viruses possess great adaptability and can change in a short time in order to evade the immune system. Enveloped viruses can cause persistent infections.
Contents
1 Enveloped examples
1.1 DNA viruses
1.2 RNA viruses
1.3 Retroviruses
2 Nonenveloped examples
2.1 DNA viruses
2.2 RNA viruses
3 See also
4 References
5 External links
Enveloped examples[edit]
Classes of enveloped viruses that contain human pathogens:
DNA viruses[edit]
Herpesviruses
Poxviruses
Hepadnaviruses
RNA viruses[edit]
Flavivirus
Togavirus
Coronavirus
Hepatitis D
Orthomyxovirus
Paramyxovirus
Rhabdovirus[2]
Bunyavirus
Filovirus
Retroviruses[edit]
Retroviruses
Nonenveloped examples[edit]
Classes of nonenveloped viruses that contain human pathogens:
DNA viruses[edit]
Adenoviridae
Papillomaviridae
RNA viruses[edit]
Picornaviridae
See also[edit]
Bacterial capsule
Cell envelope
References[edit]
Jump up ^ "CHAPTER #11: VIRUSES". Archived from the original on 2008-11-10. Retrieved 2008-11-07.
Jump up ^ "The Rabies Virus". CDC. Archived from the original on 2017-01-18. Retrieved 2008-11-07.
External links[edit]
"Virus Structure". Molecular Expressions: Images from the Microscope. Retrieved 2007-06-27.
show
v
t
e
Microbiology: Virus
Components
Viral envelope
Capsid
Viral protein
Viral life cycle
Viral entry
Viral replication
Viral shedding
Virus latency
Viroplasm
Genetics
Reassortment
Antigenic shift
Antigenic drift
Phenotype mixing
By host
Bacteriophage
Virophage
Mycovirus
Plant virus (Plant to Human)
Animal virus
Human virome
Archea virus
Amoeba virus
Other
Viral disease
Helper virus
Laboratory diagnosis of viral infections
Viral load
Virus-like particle
Virus quantification
Antiviral drug
Neurotropic virus
Oncovirus
Social history of viruses
Satellite virus
Giant virus
show
v
t
e
Viral proteins (early and late)
DNA
Herpes simplex
Herpes simplex virus protein vmw65
HHV capsid portal protein
Hepatitis B
HBsAg
HBcAg
HBeAg
HBx
Hepatitis B virus DNA polymerase
Epstein–Barr
EBNA-1
EBNA-2
EBNA-3
LMP-1
LMP-2
EBER
RNA
Rotavirus
VNPs: NSP1
NSP2
NSP4
NSP5
NSP6
Influenza
capsid:
matrix protein
M1 protein
viral envelope
M2 protein
glycoprotein:
Influenza hemagglutinin
Neuraminidase
Parainfluenza
Parainfluenza hemagglutinin-neuraminidase
Mumps
Mumps hemagglutinin-neuraminidase
Measles
Measles hemagglutinin
RSV
Respiratory syncytial virus G protein
Hepatitis C
VSPs:
E1
E2
VNPs:
P7
NS2
NS3
NS4A
NS4B
NS5A
NS5B
RT
Structure and genome of HIV
VSPs:
gag
pol
Integrase
Reverse transcriptase
HIV-1 protease
env
gp120
gp41
VRAPs:
transactivators
Tat
Rev
Vpr
Nef
Vif
Vpu
Fusion protein
Gag-onc fusion protein
Other
B13R
Retrieved from "https://en.wikipedia.org/w/index.php?title=Viral_envelope&oldid=860715634"
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