1. Chapter 23: Metamorphic Textures
Textures are small-scale penetrative features
Relict Textures
Inherited from original rock
“Blasto-” = relict
Any degree of preservation
Pseudomorphs of minerals or pre-metamorphic textures/structures
Relict bedding by alt qtz & Al-rich layers or opaques
Blasto-porphyritic
Confusion with suffix “-blast” meaning of true metamorphic origin
Porphyroblast

2. Chapter 23: Metamorphic Textures
The Processes of Deformation, Recovery, and Recrystallization
Cataclastic Flow
Mechanical fragmentation and sliding, rotation of fragments
Crush, break, bend, grind, kink, defm twins, undulose extinction, shredding of micas, augen, mortar, etc.
Technically not metamorphic
Products: fault gouge, breccia, “cataclasite”

3. Chapter 23: Metamorphic Textures
The Processes of Deformation, Recovery, and Recrystallization
Pressure Solution
Pressure solution in grains affected by a vertical maximum stress and surrounded by a pore fluid.
Figure 23-2 a. Highest strain in areas near grain contacts (hatch pattern). b. High-strain areas dissolve and material precipitates in adjacent low-strain areas (shaded). The process is accompanied by vertical shortening. c. Pressure solution of a quartz crystal in a deformed quartzite (s1 is vertical). Pressure solution results in a serrated solution surface in high-strain areas (small arrows) and precipitation in low-strain areas (large arrow). ~ 0.5 mm across. The faint line within the grain is a hematite stain along the original clast surface. After Hibbard (1995) Petrography to Petrogenesis. Prentice Hall.

4. Chapter 23: Metamorphic Textures
Plastic Intracrystalline Deformation
No loss of cohesion
Several processes may operate simultaneously
Defect migration
Slip planes
Dislocation glide
Deformation twinning

5. Chapter 23: Metamorphic Textures
Recovery
Loss of stored strain energy by vacancy migration, dislocation migration and annihilation
Polygonization- general term for formation of low-strain subgrains
Cataclasis + recrystallization (delicate interplay)
Cataclasis promotes recrystallization- lattice strain E & smaller crystals

6. Chapter 23: Metamorphic Textures
Recrystallization
Grain boundary migration
Subgrain rotation
Solid-state diffusion creep at higher T
Crystalplastic deformation (general term)
Grain boundary sliding and area reduction
Coalescence- recovery and recrystallization by which large grains form by the addition of smaller strained grains by grain boundary migration
Coalescence- general term for the collective process of recovery and recrystallization by which large grains form by the addition of smaller strained grains by grain boundary migration
Building back up following polygonization which reduces

7. Chapter 23: Metamorphic Textures
Dislocation migration forms two strain-free subgrains
Figure Illustration of a recovery process in which dislocations migrate to form a subgrain boundary. Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.

8. Chapter 23: Metamorphic Texturesb
Figure 23-4 a. Undulose extinction and (b) elongate subgrains in quartz due to dislocation formation and migration Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.

9. Recrystallization by grain boundary migration and sub-grain rotation
Bulging -> serrated boundaries
Figure 23-7a. Recrystallized quartz with irregular (sutured) boundaries, formed by grain boundary migration. Width 0.2 mm. From Borradaile et al. (1982).
Figure Recrystallization by (a) grain-boundary migration (including nucleation) and (b) subgrain rotation. From Passchier and Trouw (1996) Microtectonics. Springer-Verlag. Berlin.

10. High-Strain Metamorphic Textures (shear zones)
Truly cataclastic where shallow- narrow fault zone with gouge, breccia
As -> deeper get wider, more distributed, more ductile component
Figure Schematic cross section through a shear zone, showing the vertical distribution of fault-related rock types, ranging from non-cohesive gouge and breccia near the surface through progressively more cohesive and foliated rocks. Note that the width of the shear zone increases with depth as the shear is distributed over a larger area and becomes more ductile. Circles on the right represent microscopic views or textures. From Passchier and Trouw (1996) Microtectonics. Springer-Verlag. Berlin.

11. Chapter 23: Metamorphic Textures
High-Strain Metamorphic Textures
Concentrate on cataclastic > ductile (shallower)
Break, crack, bend, crush, rotate
Slip and shredding of phyllosilicates
Clasts- broken remnants
Porphyroclast- larger remnant in finer crush matrix
Mortar texture
Ribbons
Pseudotachylite

12. a
Progressive mylonitization of a granite, San Gabriel Mts, California
Excellent mortar in (b) b
Figure Progressive mylonitization of a granite. From Shelton (1966). Geology Illustrated. Photos courtesy © John Shelton.

13. c
Grain-size reduction
Increased foliation
Ribbon texture is forming in both
(d) is a classic ultramylonite d
Figure Progressive mylonitization of a granite. From Shelton (1966). Geology Illustrated. Photos courtesy © John Shelton.

14. Nice simple classification based on textures

15. An alternative classification that attempts to consider the processes
Good for understanding the processes, but not for naming rocks
Figure Terminology for high-strain shear-zone related rocks proposed by Wise et al. (1984) Fault-related rocks: Suggestions for terminology. Geology, 12,

16. Chapter 23: Metamorphic Textures
Textures of Contact Metamorphism
Typically shallow pluton aureoles (low-P)
Crystallization/recrystallization is near-static
Monomineralic with low D surface energy ® granoblastic polygonal
Larger D S.E. ® decussate
Isotropic textures (hornfels, granofels)
Relict textures are common
May be some stress due to moderate P or emplacement of the pluton
Minerals are often equidimensional-
Quartz and carbonates may be isotropic even when regionally met and other minerals foliated
Elongated minerals typically randomly oriented

17. Progressive thermal metamorphism of a diabase (coarse basalt)
Progressive thermal metamorphism of a diabase (coarse basalt). From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Progressive thermal metamorphism of a diabase (coarse basalt)
Incipient met- lots of relict textures from diabase
Plag -> albitic so loses Ca and Al (Ca -> calcite)
Augite hydrates -> chlorite, actinolite

18. Progressive thermal metamorphism of a diabase (coarse basalt)
Progressive thermal metamorphism of a diabase (coarse basalt). From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Stage 2- closer to igneous body- textures now metamorphic, thoroughly recrsytallized
Epidote forms as more Ca released

19. Progressive thermal metamorphism of a diabase (coarse basalt)
Progressive thermal metamorphism of a diabase (coarse basalt). From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Warmer yet, Actinolite, Chlorite, Epidote, Calcite become unstable as Hornblende and more calcic plagioclase become stable
Note coarser grain size as well

20. Progressive thermal metamorphism of a diabase (coarse basalt)
Progressive thermal metamorphism of a diabase (coarse basalt). From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Right up against gabbro body (hot), dehydrate at high grade -> Cpx + Plagioclase rock
Note that mineralogy is now ~ same as original diabase, but the texture is completely different

21. Progressive thermal metamorphism of slate. From Best (1982)
Progressive thermal metamorphism of slate. From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Progressive thermal met of slate- pelite
1) Original slate texture- already low-grade regional met.

22. Progressive thermal metamorphism of slate. From Best (1982)
Progressive thermal metamorphism of slate. From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Coarser
Random (isotropic) fabrics
Low-P minerals- And + Crd (pelite mineralogy very sensitive to P and T)
Poikiloblasts are common

23. Progressive thermal metamorphism of slate. From Best (1982)
Progressive thermal metamorphism of slate. From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Higher T -> coarser grains and less porphyroblastic
Random texture
New hi-T mineral: sillimanite coexists here with andalusite implying what?

24. The Crystalloblastic Series
Most Euhedral
Titanite, rutile, pyrite, spinel
Garnet, sillimanite, staurolite, tourmaline
Epidote, magnetite, ilmenite
Andalusite, pyroxene, amphibole
Mica, chlorite, dolomite, kyanite
Calcite, vesuvianite, scapolite
Feldspar, quartz, cordierite
Least Euhedral
Crystalloblastic Series
Differences in development of crystal form among some metamorphic minerals. From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.

25. Figure 23-9. Typical textures of contact metamorphism
Figure Typical textures of contact metamorphism. From Spry (1969) Metamorphic Textures. Pergamon. Oxford.

26. c. Fig. 23-10 Grain boundary energy controls triple point angles
a) A-A GBE > A-B -> larger dihedral angle
b) A-A GBE < A-B -> smaller dihedral
c) Sketch of plag-cpx in which cpx has lower angle
Figure a. Dihedral angle between two mineral types. When the A-A grain boundary energy is greater than for A-B, the angle  will decrease (b) so as to increase the relative area of A-B boundaries. Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall. c. Sketch of a plagioclase (light)-clinopyroxene (dark) hornfels showing lower dihedral angles in clinopyroxene at most cpx-plag-plag boundaries. (c. from Vernon, 1976) Metamorphic Processes: Reactions and Microstructure Development. Allen & Unwin, London.

27. a
Figure Drawings of quartz-mica schists. a. Closer spacing of micas in the lower half causes quartz grains to passively elongate in order for quartz-quartz boundaries to meet mica (001) faces at 90o. From Shelley (1993). b. Layered rock in which the growth of quartz has been retarded by grain boundary “pinning” by finer micas in the upper layer. From Vernon, 1976) Metamorphic Processes: Reactions and Microstructure Development. Allen & Unwin, London. b
Micas have high surface energy -> Q-Q boundaries meet mica at 90o
Also closer spacing of micas + 90o angle -> elongation and foliation to Q layers
b) Finer micas “pin” quartz to finer grain sizes

28. Metamorphic Textures
Contact overprint on earlier regional events are common
Thermal maximum later than deformational
Separate post-orogenic (collapse) event
Nodular overprints
Spotted slates and phyllites

29. a b
Figure Overprint of contact metamorphism on regional. a. Nodular texture of cordierite porphyroblasts developed during a thermal overprinting of previous regional metamorphism (note the foliation in the opaques). Approx. 1.5 x 2 mm. From Bard (1986) Microtextures of Igneous and Metamorphic Rocks. Reidel. Dordrecht. b. Spotted phyllite in which small porphyroblasts of cordierite develop in a preexisting phyllite. Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.

30. Depletion haloes
Figure Light colored depletion haloes around cm-sized garnets in amphibolite. Fe and Mg were less plentiful, so that hornblende was consumed to a greater extent than was plagioclase as the garnets grew, leaving hornblende-depleted zones. Sample courtesy of Peter Misch. Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.
Depletion halo around garnet porphyroblast. Boehls Butte area, Idaho
Progressive development of a depletion halo about a growing porphyroblast. From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.

31. Metamorphic Textures Textures of Regional Metamorphism
Dynamothermal (crystallization under dynamic conditions)
Orogeny- long-term mountain-building
May comprise several Tectonic Events
May have several Deformational Phases
May have an accompanying Metamorphic Cycles with one or more Reaction Events

32. Metamorphic Textures Textures of Regional Metamorphism
Tectonite- a deformed rock with a texture that records the deformation
Fabric- the complete spatial and geometric configuration of textural elements
Foliation- planar textural element
Lineation- linear textural element
Lattice Preferred Orientation (LPO)
Dimensional Preferred Orientation (DPO)

33. Progressive syntectonic metamorphism of a volcanic graywacke, New Zealand. From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Progressive syntectonic metamorphism of a volcanic graywacke, NZ
Both plag and Kfs in isotropic matrix
Alteration to fine sericite and secondary Ca-Al silicates

34. Progressive syntectonic metamorphism of a volcanic graywacke, New Zealand. From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Pervasive foliation develops due mostly to shear
Grain size reduction
Porphyroclasts common and rounded
Matrix recrystallized and new minerals form (Qtz, Ep, Sericite, Ab, Chl)
Chl & Ser enhance foliation

35. Progressive syntectonic metamorphism of a volcanic graywacke, New Zealand. From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Fine-grained schist with larger crystals- no relict gy textures
Good muscovite and biotite define schistosity
Some metamorphic differentiation to layering
Qtz and Ab are polygonal mosaic in mica-free layers (even though dynamothermal)

36. Progressive syntectonic metamorphism of a volcanic graywacke, New Zealand. From Best (1982). Igneous and Metamorphic Petrology. W. H. Freeman. San Francisco.
Good schist with coarser grains
More enhanced segregation into layers
Plag no longer Ab- accepts more Ca at higher T
Garnet is a new isograd mineral

37. Fig 23-21 Types of foliations
a. Compositional layering
b. Preferred orientation of platy minerals
c. Shape of deformed grains
d. Grain size variation
e. Preferred orientation of platy minerals in a matrix without preferred orientation
f. Preferred orientation of lenticular mineral aggregates
g. Preferred orientation of fractures
h. Combinations of the above
Note in (e) that linear minerals may also define a foliation if randomly oriented in a plane
Use S-surface terminology So – S1 – S2 – S3 …
Figure Types of fabric elements that may define a foliation. From Turner and Weiss (1963) and Passchier and Trouw (1996).

38. Figure A morphological (non-genetic) classification of foliations. After Powell (1979) Tectonophys., 58, 21-34; Borradaile et al. (1982) Atlas of Deformational and Metamorphic Rock Fabrics. Springer-Verlag; and Passchier and Trouw (1996) Microtectonics. Springer-Verlag.

39. Figure (continued)

40. a b
Continuous schistosity by dynamic recrystallization of biotite, muscovite, and quartz
Minerals are entirely strain-free so crystallization outlasted deformation
Figure Continuous schistosity developed by dynamic recrystallization of biotite, muscovite, and quartz. a. Plane-polarized light, width of field 1 mm. b. Crossed-polars, width of field 2 mm. Although there is a definite foliation in both samples, the minerals are entirely strain-free.