2. 1.Warm 2.Yes, A = 10 km/s, B = 5 km/s 3. List at least two of the problems associated with seismic tomography Poor source/receiver arrangement, errors in time picks, errors in earthquake locations, can ’ t resolve sharp contrasts 4.Rayleigh number: Viscosity,  Coefficient of thermal expansion,  Thermal diffusivity,  Temperature contrast,  T: E

4. Convection and the mantle Last time –Phase changes and their dependence on pressure/temperature Claudius-Clapeyron equation –How are phase transitions affected by lateral temperature changes? –How do phase transitions affect convection?

6. Mg 2 SiO 4 : Forsterite (Olivine), ~60% of mantle  ->  ->  -> perovskite 660410520? Olivine spinel

7. Depth One chemical composition, Pressure-dependent change in structure Graphite&diamonds consistent with whole mantle convection Velocity jump

8. dP/dT > 0 dP/dT < 0 (exothermic) (endothermic)

9. Subducting slabs Plumes From plumes.org

10. Tetzlaff et al, 2000

12. Back to tomography Neat results –First- order: Ocean slabs cold Problems –Source/receiver spacing Particularly bad in oceanic islands (smearing) –“Kernel” Banana-doughnut Van Der Hilst, 2002

13. Back to tomography Neat results –First- order: Ocean slabs cold Problems –Source/receiver spacing Particularly bad in oceanic islands (smearing) –“Kernel” Banana-doughnut Van Der Hilst, 2002

14. Earthquake location: High frequency

15. More impulsive signals -> larger range of sines and cosines required Noisy data, instrument response often mean only long-wavelength parts of seismogram are useful Fourier transforms: Any signal =  sines, cosines

16. With ray paths, we only consider the first arrival (requiring infinite frequencies) Energy that goes off the main path and takes longer is not considered, even if it alters the shape of the wave + =

17. Brian Amberg, wiki commons

19. With waveform cross-correlation, the whole waveform is used, including effects from signal that arrives a bit later. Waveform cross-correlation allows comparison of onset times using more than just the first arrival Called “finite frequency” since we don’t necessarily have the infinite range of frequencies that are needed to reproduce sharp pulses

20. From “Dahlen for dummies”, available online

21. Banana-Donut kernels

22. Requires: –Good first guess at model –Good constraints on source size, location –Big computers Results in: –More accurate models of mantle structure –More precise models, including better resolution of potential plumes/slabs (Montelli found many more plumes!) P PP

23. D’’

24. Seismic phases used in exploring D ” Seismic-wave ray-paths from a deep focus source (circle) to a receiver (triangle). Core-grazing phases provide sensitivity to lateral heterogeneity and anisotropy in the D ” region. D ” triplication phases (from a discontinuous increase in velocity with depth) constrain the depth and strength of any discontinuities. Phases used to study the “ ultra low velocity zone ” (ULVZ) at the base of D ” include short-period reflections (PcP) and conversions (ScP), as well as the long-period SKS phase and its associated SPdKS phase (involving P energy diffracted along the core).

25. Alaska and the Caribbean Abrupt increase in Vs Negative gradients in D ’’ Relatively cold in D ’’ Shear wave splitting at top of discontinuity (shown as fluctuations, may be caused by melt) No ultra low velocity zone (ULVZ) Central Pacific region No strong discontinuity, but neg. gradient Relatively hot in D ’’ Thick, pronounced ULVZ (5-30% decrease) Laterally variable anisotropy close to base (fluctuations) The main classes of D" shear-wave velocity structures. Schematic shear-wave velocity structures, shown as per cent deviations (V S )

26. Spatial patterns of seismological characteristics of the CMB boundary layer a, Regions with detectable ultra-low- velocity zone (ULVZ) in red, and sampled regions that lack evidence of any ULVZ are shown in blue. b, Regions with shear-wave anisotropy in D ” are shown.

27. The chemical heterogeneities schematically shown here could be due to: Partial melting core–mantle reaction products, slab-associated geochemical heterogeneities

28. Attenuation of seismic waves From: Myers et al. Some materials (e.g., hot and/or with lots of fluids) dampen seismic waves more than others Seismic waves from South America felt more strongly in Canada than in Salt Lake City Example from South America Key: Independent evidence, complementary to observed P and S wave travel times

29. Global maps of attenuation At shallow depths, similar to velocity maps: low velocities and attenuation beneath ridges; high values below continents Evidence for super plume beneath south Pacific Very difficult to resolve small scale structures like individual plumes Depends on many things, including heat flow….. From:Romanowicz and Gung, 2002

30. Global Heat Flow From: Pollack et al., 1993 Highs at Mid-ocean ridges Lows mostly over continents Think: convection heat vs. radiogenic heat? Compare with solar radiation: ~1400 W/m^2, top of atmosphere Total terrestrial heat flux average: 0.087 W/m^2 Total Power ~40 TW

31. Measuring heat flow Simple equation, hard to measure Need:  T/x –T at two depths –But… Hole disturbs T May have to wait a long time Local effects, advection? Topography? K = thermal conductivity A=area  T/x = temp gradient

32. Measuring heat flow Simple equation, hard to measure Need: k –Can be measured in lab on real sample –Predicted based on lithology –Hard for marine samples, because pore fluids, compaction during extraction K = thermal conductivity A=area  T/x = temp gradient

33. Goal: steady-state heat flow Problems: –Seasonal/daily T gradient depends on surface temperature too T cycles penetrate to various depths, w/ various magnitudes (take geodynamics) –Rapid sedimentation or erosion If dT/dz is perturbed completely within the region sampled, estimates of heat flow will be biased Measuring heat flow

34. North American Heat Flow From:Blackwell et al., 2004 East of the Rockies controlled by: 1. ground water flow, sediments (e.g. Dakota high, Mississippi Delta low) 2. Crustal radioactivity (e.g., New England White mountains) Complex effects of subduction: highs in volcanic arc, lows right above slab High heat flow throughout west from various causes (Yellowstone, Rio Grande Rift, Salton Trough, Basin and Range)