Composition. Physical Properties
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1 Composition Physical Properties
2 Summary The Earth is a layered planet The layers represent changes in composition and physical properties The compositional layers are the Crust, Mantle and Core The physical layers are the Lithosphere, Asthenosphere, Mesosphere, Outer Core and Inner Core Nearly all of this is known as the result of indirect observations, mostly through interpretation of seismic waves generated by earthquakes The Crust is divided into Oceanic crust, which is thinner, more dense, richer in iron and magnesium (Mafic) minerals and relatively young; And Continental crust, which is thicker, less dense, richer in silicon and aluminum (Felsic) minerals and relatively young;
3 Summary (continued) The Mantle is composed of dense, mafic silicates (Peridotites) The Core is composed of iron There is a solid inner core and an outer liquid core that spins generating a magnetic field The speed and refraction of seismic waves is generally used to interpret the inner structure and composition of the Earth There are also a few samples of rocks from the mantle in volcanics, kimberlite pipes, and in oceanic crust Aside from seismic studies, we also can explore the subsurface using studies of gravitational and magnetic anomalies And finally, due to Isostasy continental mountains are inferred to have deep roots.
4 The Interior of the Earth The interior of the Earth must be studied indirectly Examples of upper mantle fragments brought up by volcanic eruptions and kimberlite pipes, or scraped off onto continents by subducting oceanic plates Deepest drillhole reached about 12 km, but did not reach the mantle Geophysics is the branch of geology that studies the interior of the Earth
5 Journey to the Center of the Earth, Jules Verne The Mohole Project. Finally abandoned after reaching 12 km
6 Earth s Internal Structure The solid Earth has a layered structure Layers defined by composition and physical properties Compositional layers crust - mantle - core Physical layers lithosphere - asthenosphere - mesosphere - outer core - inner core
7 Composition Physical Properties
8 Crust Compositional Layers Outermost compositional layer Definite change in composition at the base of the crust Crust may be divided into 2 types Continental crust Oceanic crust
9 Crust Compositional Layers Continental crust Thicker than oceanic crust - up to 90 km Less dense g/cm 3 Strongly deformed Contains portions that are very old; up to 3.8 Billion years
10 Crust Oceanic crust Compositional Layers Thinner than continental crust - about 8 km More dense g/cm 3 Comparatively undeformed, i.e. no folded and faulted mountains Much younger - < 200 million years old Composed of basalt, (contains olivine)
11 Crustal Properties Crust Density Composition Thickness Age continental ~2.8 g/cm 3 Felsic Thick: km Old: up to 4 Byrs oceanic ~3.2 g/cm 3 Mafic Thin: 2-10 km Young: <200 Mys
12 Compositional Layers Mantle Largest layer in the Earth 2900 km thick 82% by volume 68% by mass Composed of silicate rocks with abundant iron and magnesium: Mafic Density ranges from 3.2 to 5 g/cm 3 Fragments found in some volcanic rocks, kimberlite pipes, and oceanic rocks scraped off onto the continent during subduction
13 Compositional Layers Core (inner and outer) Central mass about 7000km in diameter Average density of 10.8 g/cm 3 16% by volume, 32% of mass Composition Density of Earth, composition of meteorites and the Earth s magnetic field requires largely Metallic Iron plus other minor elements, e.g. Sulfur, Silicon, Nickel, etc.
14 Physical Layers Lithosphere The rock layer Crust + upper portion of the mantle Solid & rigid Thickness ranges from 10 km beneath oceans to 300 km in continental areas
15 Physical Layers Asthenosphere Upper layer in the mantle Temperature and pressure combine to allow rock to partially melt Rocks are soft and plastic They flow and are easily deformed Results in a low velocity zone for seismic waves Boundary with lithosphere is defined by mechanical properties, not composition
16 Physical Layers Mesosphere The region between the asthenosphere and the core Higher pressure offsets higher temperatures Rocks gain rigidity and mechanical strength
17 Physical Layers Outer Core ~2270 km thick Liquid, flows Flow creates magnetic field Inner Core ~1200 km thick Solid
18 The Earth s Magnetic Field
19
20 How you can use seismic waves to explore the interior of the Earth
21 No refraction in homogeneous materials Fig. 11-4a, p. 341
22 Refraction in heterogeneous materials Fig. 11-4b, p. 341
23 Seismic waves in a homogeneous planet
24 Seismic waves in a differentiated planet
25 Fig. 11-4c, p. 341
26 Fig , p. 346
27 Fig. 11-9c, p. 345
28 Fig. 11-9b, p. 345
29 Seismic Structure of the Earth Seismic wave velocities vary with depth Variation with depth is not smooth Discontinuities at certain depths represent discrete changes in structure, chemistry and phase (liquid/solid) of minerals in the mantle
30 Seismic Structure of the Earth Mohorovicic Discontinuity (Moho) First discovered by Andrija Mohorovicic Occurs between 5 and 70 km deep Represents the base of the crust, i.e. the crust/mantle boundary Compositional change from feldspar rich to olivine rich rocks causes a significant increase in seismic velocities Causes refracted seismic waves
31 These waves travel are refracted here and here. Even though they travel farther, they arrive first. Therefore they have traveled faster
32 Seismic Structure of the Earth Low-velocity zone Layer from ~100 to 250 km deep Seismic velocities usually increase with depth In the low velocity zone velocity slows by ~ 6% Caused by partially molten mantle that slows seismic waves May form a slippery layer that the overlying crust slides upon
33 Internal structure of the Earth
34 Movement in the Earth In the core 3-D models and magnetic field suggest flowing molten iron with likely internal convection resulting in occasional chaotic reversals In the mantle Investigations show a complex convection system occurring in the entire mantle system, including an active D layer at the core/mantle boundary
35 Convection in the Earth The ULVZ and the D layer
36 The Ultra Low Velocity Zone (ULVZ) and the D layer; the stormy layer at the Core/Mantle boundary Source of mantle plumes and hot spots?
37
38 The Core Core composition inferred from its calculated density, physical and electro-magnetic properties, and composition of meteorites Iron metal (liquid in outer core and solid in inner core) best fits observed properties Iron is the only metal common in meteorites Core-mantle boundary (D layer) is marked by great changes in seismic velocity, density and temperature Hot core may melt lowermost mantle or react chemically to form iron silicates in this seismic wave ultralow-velocity zone (ULVZ)
39 Meteorites record the composition of the early solar system ~4.6 billion years old Three types of meteorites Iron (mostly iron, some nickel and other metals Stony (most common; silicate minerals: plagioclase, olivine, pyroxene) Stony-iron (mixed composition) One unusual type is a carbonaceous chondrite, which can contain up to 5% organic carbon, i.e. hydrocarbons, amino acids.
40 Heat Within the Earth Geothermal gradient - temperature increase with depth into the Earth Tapers off sharply beneath lithosphere Due to steady pressure increase with depth, increased temperatures produce little melt (mostly within asthenosphere) except in the outer core Heat flow - the gradual loss of heat through Earth s surface Major heat sources include original heat (from accretion and compression as Earth formed) and radioactive decay Locally higher where magma is near surface Same magnitude, but with different sources, in the oceanic (from mantle) and continental crust (radioactive decay within the crust)
41
42 Fig. 11-1a, p. 336
43 Fig. 11-1b, p. 336
44 Fig. 11-7, p. 343
45 Fig. 11-8a, p. 344
46 Fig. 11-8b, p. 344
47 Fig , p. 347
48 Fig a, p. 347
49 Fig b, p. 347
50 Gravitational Anomalies Dense and therefore exerting more gravitational attraction
51 Gravitational Anomalies Common way to explore for faults and therefore water in desert areas such as the southwest US
52 Gravitational Anomalies Common way to explore for salt domes and therefore oil in the Gulf Coast area
53 Fig a, p. 350
54 Fig b, p. 350
55 Fig , p. 350
56 The mass of the volume of water displaced is equal to the total mass of the iceberg 10% of the mass 10% of the mass 90% of the mass 90% of the mass Fig b, p. 350
57 Fig a, p. 350
58 Fig a, p. 351
59 Fig b, p. 351
60 Fig c, p. 351
61 Fig , p. 351
62 Fig , p. 351
63 Fig a, p. 351
64 Fig b, p. 351
65 Fig c, p. 351
66 Fig a, p. 351
67 Fig , p. 352
68 Fig , p. 352
69 Magnetic Anomalies Fig a, p. 353
70 Magnetic Anomalies Fig b, p. 353
71 Magnetic Anomalies Fig c, p. 353
72 Earth s Internal Structure Seismic waves have been used to determine the three main zones within the Earth: the crust, mantle and core The crust is the outer layer of rock that forms a thin skin on Earth s surface The mantle is a thick shell of dense rock that separates the crust above from the core below The core is the metallic central zone of the Earth
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