Isostasy, gravity, magnetism, and internal heat Earth’s gravity field

  • View
    241

  • Download
    3

Embed Size (px)

Text of Isostasy, gravity, magnetism, and internal heat Earth’s gravity field

  • Slide 1
  • isostasy, gravity, magnetism, and internal heat Earths gravity field
  • Slide 2
  • isostasy equilibrium of adjacent blocks of brittle crust floating on underlying upper mantle outer layers of Earth divided into 2 based on their strength lithosphere: rigid, solid outer layer (brittle) --strong crust and uppermost mantle DO NOT CONFUSE WITH CRUST AND MANTLE WHICH ARE BASED ON COMPOSITION asthenosphere: underlying denser, heat-softened, partially melted (plastic) -- weak upper mantle transition from lithosphere to asthenosphere reflects temperature and rocks response to increased temperature
  • Slide 3
  • isostasy equilibrium of adjacent blocks of brittle crust floating on underlying upper mantle i.e. mass above a certain depth must be the same think of wood blocks in water block that sticks up higher also extends farther in water density of wood < density of water for masses to be the same above the isostatic compensation depth: compensation depth mass in column 1 = mass in column 2 masses in both columns in 2 dimensions equal (density wood x thickness wood) + (density water x thickness water) density water > density wood wood that replaces water in the column must be thicker than water it replaces
  • Slide 4
  • isostasy continental crust is less dense than oceanic crust mass in column 1 = mass in column 2 = mass in column 3 density mantle > density oceanic crust > density continental crust crust is less dense than mantle same concept as wood blocks applies to lithospheric blocks (crust and uppermost mantle) floating on asthenosphere above the compensation depth compensation depth if more mantle in column -- column will be thinner if more continental crust in column -- column will be thicker implication is that mountains have roots -- crust is thicker below them
  • Slide 5
  • isostasy a more detailed view of density differences include sea water & sediments
  • Slide 6
  • isostasy leads to isostatic adjustment if mass is redistributed erosion redistributes rock from mountain (high) to sediment deposited in basin (low) less mass on mountain causes uplift of crust below mountain (thins and rises) and subsidence of basin as mass of sediment is added note mountain and crustal root below it erosion of mountain as mountain erodes, column becomes shorter thus, mantle mass in column increases over time (mass A = mass B = mass C) ABC A B C X mantle crust AX effect on mass columns
  • Slide 7
  • isostasy see isostatic adjustment today from load of glaciers on crust during last glaciation and unloading from melting (possible because response of asthenosphere is slow) process is called post-glacial rebound
  • Slide 8
  • isostasy post-glacial rebound still occurs in Canada & northern Europe i.e. crust is rising -- (not isostatically balanced) (can measure uplift rates with highly precise GPS receivers--mms/yr) amount of uplift since glaciation
  • Slide 9
  • Polar Glaciers Melting Animation From: http://www.uni-geophys.gwdg.de/~gkaufman/work/onset/onset_ice3g.html
  • Slide 10
  • gravity gravitational force between two objects determined by their masses and distance between them
  • Slide 11
  • gravity differences in density of materials (rocks) in Earths interior produces small differences in local gravity field (anomalies) can be measured with a gravimeter (attraction of spring to mass) dense material attracts and extends spring void (cave) has no mass to attract spring mass uniform and spring is neutral can find buried, dense things (abandoned gas station tanks) and empty spaces (caves -- dont build)
  • Slide 12
  • gravity density differences also occur over larger areas: mountains mass above compensation depth is uniform (isostatically balanced) --no excess or deficiency in mass; no gravity anomalies-- compensation depth
  • Slide 13
  • gravity mass above compensation depth is not uniform -- excess mass of dense mantle below mountain (no crustal root) compensation depth generates increased gravity and, thus, a positive gravity anomaly
  • Slide 14
  • gravity mass above compensation depth is not uniform -- deficiency of mass below low area (too much crust) compensation depth generates decreased gravity and, thus, a negative gravity anomaly
  • Slide 15
  • Earths gravity field measured from space mass in Earth pulls on satellites as they orbit, causing wobbles in orbit paths, which are measured --amount of wobble related to amount of mass-- GRACE --NASA-- mission to examine Earths gravity field
  • Slide 16
  • Earths magnetic field surrounds the Earth has north and south magnetic poles is detected by compasses is recorded in rocks and minerals as they cool is generated in the Earths liquid outer core as it spins and produces electrical currents Earths field similar to that for bar magnet (left) magnetic N and S is not the same as geographic N and S poles (bar magnet tilted)
  • Slide 17
  • Earths magnetic field changes through time change in magnetic north relative to true north 1580-1970 1831-2001 migration of magnetic north consequence of rotation of outer core
  • Slide 18
  • N S Earths magnetic field reverses over time (north and south poles flip) --magnetic field lines reverse-- normal polarity: north is north and south is south reversed polarity: north is south and south is north after next reversal, compass needle will point south
  • Slide 19
  • Earths magnetic field how do rocks and minerals acquire magnetism? rocks and minerals at high temperatures (e.g. molten) must cool through their Curie temperatures above Curie temperature, atoms are random below Curie temperature, atoms align in domains that are independent of each other below Curie temperature, atoms align with magnetic field if one is present (e.g. Earth)
  • Slide 20
  • Earths magnetic field how do rocks and minerals acquire magnetism? rocks and minerals that cool through Curie temperature and stay below that temperature through time record magnetic field AT THE TIME OF THEIR COOLING magnetite common mineral in basalt paleomagnetism: study of ancient magnetic fields in rocks --reconstruction of past fields--
  • Slide 21
  • thick flood basalt sequence in Brazil Earths magnetic field examine thick sequences of basalts to identify reversals through time (paleomagnetism)
  • Slide 22
  • Earths magnetic field re-construct normal and reversed for lava sequence
  • Slide 23
  • Earths magnetic field create time-scale for magnetism from many observations black = normal polarity blue = reverse polarity see that lengths of magnetic periods are not uniform likely relates to turbulent flow of outer core blue = normal polarity red = reverse polarity
  • Slide 24
  • reversed (orange north) transitional (chaotic) normal (blue north) Earths magnetic field what happens during reversals? geologic evidence suggests that reversals occur quickly (a few 1000 yrs) computer simulations indicate that transitions are chaotic with many magnetic poles in odd places i.e. not N or S
  • Slide 25
  • magnetic material below adds magnetism and creates positive anomaly Earths magnetic field magnetic anomalies occur in local field from magnetic rock below surface (similar to gravity anomalies) magnetic rocks include iron ore, gabbro, granite
  • Slide 26
  • Earths magnetic field removal of magnetic material from near surface causes negative anomaly (example is normal faulting)
  • Slide 27
  • Earths internal heat geothermal gradient: temperature increases with depth in the Earth--most dramatic in crust; tapers off deeper crust: rapid increase in T (25/km) slower increase deeper (1/km) despite increase in temperature, rocks do not melt because pressure also increases with depth (big increase in T in outer core--molten)
  • Slide 28
  • Earths internal heat heat sources must be in shallow crust for crustal gradient heat flow: gradual loss of heat from interior to surface magma bodies uranium-rich igneous rock (decay of U, Th, K generates heat)
  • Slide 29
  • Earths internal heat heat flow is reasonably similar over oceans and continents heat comes from different sources in two regions continental crust: radioactive decay in granites oceanic crust: mantle sources (no granite in oceanic crust)
  • Slide 30
  • Earths internal heat observed heat flow at Earths surface shows gross patterns (red is warm; blue is cold) red at mid-ocean ridges blue over oldest parts of continents
  • Slide 31
  • Earths internal heat gradual loss of heat from interior to surface causes mantle convection as mechanism of heat transfer upwelling (rising of warm material) in mantle below mid-ocean ridges downwellling (sinking of cooled material) at subduction zones loss of heat as material moves laterally at surface