Crystal preferred orientations of olivine, orthopyroxene, serpentine, chlorite, and amphibole, and implications for seismic anisotropy in subduction zones: a review

Abstract

This study provides a comprehensive review of the crystal preferred orientation (CPO) of olivine and orthopyroxene in the upper mantle, and of several hydrous minerals in the mantle wedge and at the slab-mantle interface. It discusses the seismic anisotropy of those minerals. Water-induced CPOs of olivine produced by previous experimental studies under high pressure and temperature conditions were found in many natural rocks. It is emphasized that the strong CPOs of hydrous minerals such as serpentine, chlorite, and amphibole, play an important role in interpreting the anomalously strong seismic anisotropy observed in subduction zones.

Full text

Review
Vol. 21, No. 6, p. 985−1011, December 2017
http://dx.doi.org/10.1007/s12303-017-0045-1
pISSN 1226-4806 eISSN 1598-7477
Geosciences Journal
GJ
Crystal preferred orientations of olivine, orthopyroxene,
serpentine, chlorite, and amphibole, and implications
for seismic anisotropy in subduction zones: a review
Haemyeong Jung*
Tectonophysics Laboratory, School of Earth and Environmental Sciences, Seoul National University, Seoul 08826, Republic of Korea
ABSTRACT: This study provides a comprehensive review of the crystal preferred orientation (CPO) of olivine and orthopyroxene
in the upper mantle, and of several hydrous minerals in the mantle wedge and at the slab-mantle interface. It discusses the seismic
anisotropy of those minerals. Water-induced CPOs of olivine produced by previous experimental studies under high pressure and
temperature conditions were found in many natural rocks. It is emphasized that the strong CPOs of hydrous minerals such as ser-
pentine, chlorite, and amphibole, play an important role in interpreting the anomalously strong seismic anisotropy observed in sub-
duction zones.
Key words: crystal preferred orientation, olivine, orthopyroxene, serpentine, chlorite, amphibole, seismic anisotropy
Manuscript received June 17, 2017; Manuscript accepted September 27, 2017
1. INTRODUCTION
Rocks inside the Earth’s crust and mantle are deformed under
differential stress at high pressure and temperature conditions,
and those in the deep interior go through plastic deformation.
The minerals constituting rocks are deformed and elongated,
forming a crystal preferred orientation (CPO) or a lattice preferred
orientation (LPO). If a mineral is elastically very anisotropic, the
CPO of its aggregates can cause a significant seismic anisotropy
in the crust and the mantle. Seismic anisotropy has been observed
worldwide in the Earth’s interior (Fig. 1) and can provide important
information for understanding the evolution of the upper
mantle, mantle flow pattern, mantle dynamics, and tectonics
(Hess, 1964; Nicolas and Christensen, 1987; Silver, 1996; Ben
Ismail and Mainprice, 1998; Savage, 1999; Jung and Karato,
2001; Smith et al., 2001; Jung et al., 2006; Mainprice, 2007;
Karato et al., 2008; Long and Silver, 2008; Long and Silver, 2009;
Di Leo et al., 2012; Jung, 2012; Long, 2013; Tommasi and Vauchez,
2015; Skemer and Hansen, 2016; Zhao et al., 2016). Therefore,
studying the CPO of elastically anisotropic minerals that are
dominant in the crust and the upper mantle is essential.
In the upper mantle, the dominant minerals inside rocks are
olivine and orthopyroxene (Fig. 2a). Olivine is the most abundant
mineral and is elastically anisotropic (Birch, 1960; Verma, 1960;
Abramson et al., 1997) (Table 1). The CPO of olivine is key to
understanding the seismic anisotropy and flow pattern of the
upper mantle (Hess, 1964; Nicolas and Christensen, 1987; Ben
Ismail and Mainprice, 1998; Jung et al., 2006; Karato et al., 2008;
Cao et al., 2015; Michibayashi et al., 2016; Cao et al., 2017). In
the mantle wedge and at the slab-mantle interface, hydrous
minerals such as serpentine, chlorite, and amphibole (Figs. 2b–
d) can form from the fluids generated by the dehydration of
hydrous minerals in the subducting slab (Ulmer and Trommsdorff,
1995; Peacock and Hyndman, 1999; Pawley, 2003; Fumagalli
and Poli, 2005; van Keken et al., 2011). Many of hydrous minerals
such as chlorite, amphibole, and serpentine can be formed after
olivine meets water during exhumation in the mantle wedge
and at the interface between slab and mantle wedge. Those
hydrous minerals are known to be stable at a wide range of
pressure-temperature conditions in subdution zone (Schimidt
and Poli, 1998; Ulmer and Trommsdorf, 1995; Fumagali and
Poli, 2005) (Fig. 3). Those hydrous minerals are also known as
elastically anisotropic minerals (Aleksandrov and Ryzhova, 1961a;
Mainprice and Ildefonse, 2009; Bezacier et al., 2010; Mookherjee
*Corresponding author:
Haemyeong Jung
Tectonophysics Laboratory, School of Earth and Environmental Sci-
ences, Seoul National University, Seoul 08826, Republic of Korea
Tel: +82-2-880-6733, Fax: +82-2-871-3269, E-mail: hjung@snu.ac.kr
©
The Association of Korean Geoscience Societies and Springer 2017

986 Haemyeong Jung
http://dx.doi.org/10.1007/s12303-017-0045-1
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Fig. 1. Examples of seismic anisotropy observed worldwide. This figure shows a summary map of mantle wedge splitting of S-waves (Long
and Wirth, 2013). Arrows indicate the first‐order patterns in average fast direction; where multiple arrows are present, this indicates a spatial
transition in observed orientation (φ). Arrows are color coded by fast direction observations; magenta arrows indicate dominantly trench‐par-
allel φ, blue arrows indicate dominantly trench‐perpendicular φ, yellow arrows indicate complex and variable φ, red arrows indicate a tran-
sition from trench‐parallel φ close to the trench to trench‐perpendicular φ farther away, and green arrows indicate the opposite transition
(from trench‐perpendicular φ close to the trench to trench‐parallel φ farther away). Beneath the name of each subduction zone, the range
of observed delay times is indicated.
Tab le 1 . Seismic (elastic) anisotropy of olivine and orthopyroxene (opx)
Mineral Single crystal Poly crystal Reference
AVp (%) max. AVs (%) AVp (%) max. AVs (%)
Olivine (forsterite)
23.8 16.0 Mainprice (2007)
(a)
4.9–11.1 4.9–7.4 Jung and Karato (2001)
(a)
8.3–13.3 5.3–9.3 Michibayashi et al. (2006)
(a)
2.7–6.0 1.8–4.8 Katayama and Karato (2006)
(a)
2.6 2.9 Skemer et al. (2006)
(a)
12.0 7.0–10.4 Hidas et al. (2007)
(a)
4.5–9.8 3.2–7.0 Tasaka et al. (2008)
(a)
7.8–13.6 5.4–8.2 Jung et al. (2009a)
(a)
3.2–7.2 2.2–5.5 Jung (2009)
(a)
1.8–7.3 2.2–5.5 Ohuchi et al. (2011)
(a)
6.1–8.6 3.9–5.6 Michibayashi et al. (2012)
(a)
2.7–5.9 2.5–5.0 Jung et al. (2013)
(a)
8.8–8.9 5.3–5.7 Park et al. (2014)
(a)
1.2–3.6 2.1–3.7 Watanabe et al. (2014)
(a)
2.2–11.6 1.9–7.5 Park and Jung (2015)
(a)
1.8–3.8 1.7–2.7 Kim and Jung (2015)
(a)
5.2–9.1 8.4–8.6 Boneh et al. (2015)
(a)
11.0–13.9 10.5–14.2 Lee and Jung (2015)
(a)
1.8–7.5 1.1–5.2 Kang and Jung (2017)
(a)
Opx (enstatite)
13.7 17.6 Mainprice (2007)
(b)
2.9 2.7 Skemer et al. (2006)
(b)
1.8–5.9 2.4–4.0 Jung et al. (2010)
(b)
3.4 3.9 Jung et al. (2013)
(b)
1.2–2.3 1.5–2.5 Park and Jung (2015)
(b)
AVp: anisotropy of P-wave velocity. AVp = 100 (%) × [(Vpmax – Vpmin)/(0.5 × (Vpmax + Vpmin))], where Vpmax is the maximum P-wave velocity
and Vpmin is the minimum P-wave velocity (Birch, 1960).
AVs: anisotropy of S-wave velocity. AVs = 100 (%) × [(Vs1 – Vs2)/(0.5 × (Vs1 + Vs2))], where Vs1 is the fast S-wave velocity and Vs2 is the slow
S-wave velocity.
(a)
Elastic constants of olivine(forsterite) from Abramson et al. (1997) were used.
(b)
Elastic constants of orthopyroxene(enstatite) from Chai et al. (1997) were used.

Crystal preferred orientations of olivine and hydrous minerals 987
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and Mainprice, 2014) (Table 2); their CPOs are important for
interpreting seismic anisotropy in many subduction zones
(Katayama et al., 2009; Jung, 2011; Brownlee et al., 2013; Morales
et al., 2013; Kim and Jung, 2015; Ko and Jung, 2015; Nagaya et
al., 2016; Kang and Jung, submitted). In addition, one of the
important minerals in the middle and lower crust is amphibole,
which is also elastically anisotropic (Aleksandrov and Ryzhova,
1961a; Siegesmund et al., 1989; Weiss et al., 1999; Kaczmarek
and Tommasi, 2011; Lloyd et al., 2011; Ji et al., 2013; Ko and
Jung, 2015; Brown and Abramson, 2016; Almqvist and Mainprice,
2017). A recent experimental study under simple shear at high
pressure and temperature showed that the CPO of amphibole
(hornblende) might cause large seismic anisotropy (Ko and
Jung, 2015). Amphibole and chlorite in hydrated peridotites in
the lower part of the mantle wedge also play a key role in the
interpretation of seismic anisotropy in subduction zones (Kim
and Jung, 2015; Kang and Jung, submitted).
This work provides a comprehensive review of the experimental
studies on the CPO of olivine first. The effect of water, stress,
temperature, pressure, shear strain, and deformation history on
the CPO of olivine is presented along with the recent findings
on the CPO of olivine in natural rocks. Next, the CPOs of
orthopyroxene and serpentine are described, followed by a review
of the recent advances in the study of the CPO of hydrous minerals
including chlorite and hornblende. Finally, geophysical implications
of the results of the recent studies on the CPOs of hydrous minerals
Fig. 2. Optical photomicrographs showing deformation microstructures of natural rocks (a–e) and an experimental sample (f). (a) Mantle
xenolith (SVF-04) from Svalbard, Arctic showing olivine and orthopyroxene (Jung et al., 2009a). White arrows indicate Kink bands in olivine.
Scale bar represents 2 mm. (b) Serpentinite (VM3) from Val Malenco, Italy (Jung, 2011). Scale bar represents 0.2 mm. (c) Chlorite peridotite
(436) from Amklovdalen, SW Norway (Kim and Jung, 2015). Scale bar represents 1 mm. (d) Amphibole peridotite from Bjorkedalen, SW Nor-
way (Kang and Jung, submitted). Scale bar represents 0.5 mm. (e) Yugu peridotite (YG-10) showing ultramylonite texture in Yugu, South
Korea (Park and Jung, 2017). Scale bar represents 3 mm. (f) A back-scattered electron image of a deformed amphibolite at a high pressure
of 1 GPa and temperature of 600 °C (Ko and Jung, 2015). Arrows show the sense of shear. Ol: olivine, Opx: orthopyroxene, Ant: antigorite,
Mgt: magnetite, Chl: chlorite, Amp: amphibole, Sp: spinel, Cpx: clinopyroxene, Srp: serpentine, Hb: hornblende, Pl: plagioclase, and Il: ilmenite.

988 Haemyeong Jung
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and olivine, and the resultant seismic anisotropy are discussed.
2. STUDIES ON THE SLILP SYSTEM AND CPOs
OF OLIVINE
Early experiments on the deformation of single crystal olivine
at high pressure were performed by Rayleigh (Raleigh, 1965, 1968)
under uniaxial compression and identified active slip systems of
olivine by observing detailed microstructures such as kink bands,
slip bands, and deformation lamellae. Slip system is defined by a
slip plane and a slip direction (i.e., (010)[100] slip system refers
to a slip occurring at the (010) plane and along the [100] direction).
At low temperatures (less than 1,000 °C), the slip systems of
olivine were {110}[001], (100)[001], and (100)[010], while at the
Tab l e 2. Seismic (elastic) anisotropy of hydrous minerals.
Mineral Single crystal Poly crystal Reference
AVp (%) max. AVs (%) AVp (%) max. AVs (%)
Serpentine (antigorite)
71.2 67.6 Mainprice and Ildefonse (2009)
(a)
46.0 66.5 Bezacier et al. (2010)
(b)
38.4–46.3 24.2–32.4 Katayama et al. (2009)
(c)
10.4–31.3 8.9–36.0 Hirauchi et al. (2010)
(b)
36.8 50.5 Bezacier et al. (2010)
(b)
32.9 31.0 Soda and Takagi (2010)
(b)
23.6–31.4 22.8–36.5 Jung (2011)
(b)
7.6–8.2 14.0–36.2 Nishii et al. (2011)
(b)
5.7–27.6 4.9–33.2 Brownlee et al. (2013)
(b)
13.9–25.7 15.0–24.0 Watanabe et al. (2014)
(b)
34.2 - Nagaya et al. (2016)
(b)
Chlorite (clinochlore)
35.5 76.2 Mainprice and Ildefonse (2009)
(d)
35.5 76.2 Kim and Jung (2015)
(d)
14.9–21.1 14.5–31.7 Kim and Jung (2015)
(d)
10.3–15.2 10.6–22.8 Kim and Jung (2015)
(e)
22.3–25.2 31.6–46.2 Kang and Jung (2017)
(d)
Amphibole (hornblende)
27.2 - Kitamura (2006)
(f)
27.1 30.7 Mainprice and Ildefonse (2009)
(f)
27.1 30.7 Lloyd et al. (2011)
(f)
27.1 30.7 Ko and Jung (2015)
(f)
9.5–11.1 7.0–8.0 Siegesmund and Vollbrecht (1991)
(g)
11.4 - Barruol and Kern (1996)
(f),(g)
3.2–7.7 - Kitamura (2006)
(f),(g)
3.6–6.0 3.8–6.9 Tatham et al. (2008)
(f),(g)
7.5–14.0 4.2–8.5 Ji et al. (2013)
(g),(h)
10.2–13.5 6.9–11.2 Jung et al. (2014a)
(f)
9.0–14.6 7.6–12.1 Ko and Jung (2015)
(f)
5.7–14.0 4.1–8.5 Ji et al. (2015)
(g),(i)
11.4 6.9 Lamarque et al. (2016)
(f)
10.0–15.2 7.5–11.9 Kang and Jung (2017)
(f)
AVp: anisotropy of P-wave velocity. AVp = 100 (%) × [(Vpmax – Vpmin)/(0.5 × (Vpmax + Vpmin))], where Vpmax is the maximum P-wave velocity
and Vpmin is the minimum P-wave velocity (Birch, 1960).
AVs: anisotropy of S-wave velocity. AVs = 100 (%) × [(Vs1 – Vs2)/(0.5 × (Vs1 + Vs2))], where Vs1 is the fast S-wave velocity and Vs2 is the slow
S-wave velocity.
(a)
Elastic constants of serpentine (antigorite) from Pellenq et al. (submitted) were used.
(b)
Elastic constants of serpentine (antigorite) from Bezacier et al. (2010) were used.
(c)
Elastic constants of serpentine (lizardite) from Auzende et al. (2006).
(d)
Elastic constants of chlorite (clinochlore) from Alexandrov and Ryzhova (1961b).
(e)
Elastic constants of chlorite (clinochlore) from Mookherjee and Mainprice (2014).
(f)
Elastic constants of amphibole (hornblende) from Alexandrov and Ryzhova (1961a).
(g)
Seismic anisotropy of whole rock, amphibolite.
(h)
Elastic constants of amphibole(hornblende) from Hearmon (1984).
(i)
Elastic constants of amphibole(hornblende) from Alexandrov et al. (1974).

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high temperature of 1,000°C, the slip system was {0kl}[100],
which is the pencil glide in [100] direction (Raleigh, 1968). Later
experiments at higher pressure (up to P = 3 GPa) and temperature
(up to 1,400 °C) conditions (Carter and Avé Lallemant, 1970)
identified the slip system of olivine as (010)[100] at temperatures in
excess of 1,100 °C.
The first experimental study to determine the CPO of olivine
aggregates was conducted in the uniaxial compression mode
using a Griggs apparatus (Fig. 4a) under dry conditions (Avé
Lallemant and Carter, 1970). Olivine [010] axes were found to
be aligned subparallel to the maximum principal stress (strain
axis) orientation. Both [100] and [001] axes were aligned in a
girdle subnormal to the maximum principal stress (strain axis)
orientation. In 1995, the first simple shear deformation experiment
of olivine aggregates at the pressure of 300 MPa and temperatures of
1,200–1,300 °C was conducted using a gas-medium Paterson
apparatus under dry conditions (Zhang and Karato, 1995) and
mor e exp erimental data were pub lish ed la ter ( Zhang et a l., 200 0).
These simple shear experiments showed that olivine [010] axes
were aligned subnormal to the shear plane and [100] axes were
aligned subparallel to the shear direction under dry conditions.
2.1. Effect of Water and Stress on the CPOs of Olivine
2.1.1. Experimental study
Water has been known to affect the CPO of olivine since the
pioneering experimental study (Jung and Karato, 2001). To
understand the effect of water and stress on the CPO of olivine,
deformation experiments were conducted on olivine aggregates
Fig. 3. Stability field of hydrous minerals
in subduction zone. Stippled lines are
isotherms by thermal model (Furukawa,
1993) and bold arrows indicate flow
lines in the mantle wedge. Blue line
indicates the stability boundary of chlo-
rite in peridotite. Example of strong
CPO of chl (Kim and Jung, 2015), serp
(Jung, 2011), and amp (Ko and Jung,
2015) is shown, which is important for
the interpretation of anomalously
strong seismic anisotropy in subduction
zones. chl: chlorite, amp: amphibole
(hornblende), serp: serpentine (antigor-
ite), opx: orthopyroxene, cld: chloritoid,
lws: lawsonite, and phg: phengite. Mod-
ified after Schmidt and Poli (1998).
Fig. 4. Equipment used for high-temperature, high-pressure defor-
mation experiments on minerals and rocks. (a) Griggs apparatus (2
GPa), and (b) modified Griggs apparatus (5 GPa) at the Tectonophys-
ics Laboratory, Seoul National University, South Korea.

990 Haemyeong Jung
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in simple shear (Fig. 5), using a Griggs apparatus (Fig. 4a) at high
pressure (0.3–2.1 GPa) and temperature (1,190–1,300 °C), discovering
olivine Type-B and -C CPOs (Fig. 6a) and defining olivine Type-A,
-B, -C, and -D CPOs (Jung and Karato, 2001). The starting materials
were San Carlos olivine aggregates and single crystal olivine that
contained 10% Fe, as a representative sample of the upper mantle.
The sample was hot-pressed at 300 MPa and 1,200 °C. Experiments
were conducted under both dry and wet conditions. In wet
conditions, water was added to the sample by the dehydration of
the mixture of talc and brucite at high temperature. Sample
assembly for shear deformation experiment is shown in Figure
5. The sample was deformed at constant strain rates (9.5 × 10
–4
–
5.6 × 10
–6
s
–1
) with a shear strain of 0.6–6.3 (Jung and Karato,
2001; Katayama et al., 2004; Jung et al., 2006). Dry conditions
were defined as a water content of less than 200 ppm H/Si in single
crystal olivine without any cracks, inclusions, or grain boundaries
in the sample.
The representative CPOs of olivine produced in a simple
shear at high pressures under both dry and wet conditions are
summarized in Figure 6a and a fabric diagram of olivine is
shown in Figure 6b. Several types of olivine CPOs were found:
Type-A CPO of olivine was formed under low-stress and dry
conditions; water content in the single crystal olivine was less
than 200 ppm H/Si (Jung and Karato, 2001). The Type-A CPO
of olivine is characterized by olivine [010] axes aligned subnormal
to the shear plane and [100] axes aligned subparallel to the shear
direction, having a dominant slip system of (010)[100]. Type-B
CPO of olivine was found under high-stress and varied water
content (200 ≤C
OH
≤1200 ppm H/Si) conditions and characterized
as [010] axes aligned subnormal to the shear plane and [001] axes
aligned subparallel to the shear direction, having a dominant
slip system of (010)[001] (Jung and Karato, 2001). Type-C CPO
of olivine was observed under low-stress and water-rich conditions
with a water content of C
OH
≥700 ppm H/Si and characterized
Fig. 5. Central portion of sample assembly for a shear deformation
experiment at high pressure and temperature using a Griggs apparatus.
Fig. 6. (a) Typical CPOs of olivine showing Type-A, -B, -C, -D, -E, and
-AG (modified from Jung et al., 2006). Type-A (MIT23), Type-B (JK21),
Type-C (JK11), Type-D (SVF-49: Jung et al., 2009a), Type-E (GA25),
and Type-AG (Jung et al., 2014b). Pole figures are presented in the
lower hemisphere using an equal area projection. The sense of shear
is presented by arrows. The north (south) poles correspond to the
shear plane normal. Crystallographic orientations of ~200–650
grains of each sample were measured manually by the EBSD tech-
nique. A half-width of 30° was used to draw the pole figure. The
color coding refers to the density of data points (contours in the pole
figures correspond to the multiples of uniform distribution). (b) A
fabric diagram of olivine at P = 0.3–2.1 GPa and T ~ 1200 °C showing
the dominant fabrics as a function of water content (C
OH
) and stress
(after Jung et al., 2006). σ: differential stress, μ: shear modulus.

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as [100] axes aligned subnormal to the shear plane and [001]
axes aligned subparallel to the shear direction, having a dominant
slip system of (100)[001] (Jung and Karato, 2001). Type-D CPO
of olivine was formed under high-stress and dry conditions
and characterized as [100] axes aligned subparallel to the
shear direction and both [010] and [001] axes aligned as a
girdle subnormal to shear direction, having a dominant slip
system of {0kl}[100] (Bystricky et al., 2000; Zhang et al., 2000).
Finally, Type-E CPO of olivine was found under low-stress
and moderate water content (200 ≤C
OH
< 700 ppm H/Si)
conditions and characterized as [001] axes aligned subnormal
to the shear plane and [100] axes aligned subparallel to the
shear direction, having a dominant slip system of (001)[100]
(Katayama et al., 2004; Jung et al., 2006).
Based on the study of natural rocks, one more CPO of
olivine, Type-AG (Mainprice, 2007; Michibayashi et al., 2016),
sometimes called as axial [010] pattern (Tommasi and
Vauchez, 2015), was reported. It is characterized by [010] axes
strongly aligned subnormal to the foliation and both [100] and
[001] axes aligned subparallel to the foliation (Fig. 6a). The
Type-AG CPO of olivine was also called type A + B CPO ( type
A + type B CPO) because it can be formed under a mixed
condition (deformed in dry condition and later in wet condition,
vice versa) (Jung et al., 2014b).
2.1.2. Observation of water-induced CPOs of olivine
in natural rocks
Early studies of olivine CPOs in natural rocks were conducted
by Nicolas and Christensen (1987) and Ben Ismail and Mainprice
(1998). Since water-induced CPOs of olivine were discovered in
experimental studies (Jung and Karato, 2001; Katayama et al.,
2004; Jung et al., 2006), there has been active research on the
petrofabrics of olivine in natural rocks (Table 3). Mizukami et al.
(2004) reported on the water-induced Type-B CPO of olivine in
the peridotites in Higashiakaishiyama, southwest Japan. Frese et
al. (2003) found Type-C CPOs of olivine in prograde garnet
peridotites in Cima di Gagnone, in the Central Alps, and reported
that the fabrics formed at high water activity. Skemer et al. (2006)
also reported the Type-B CPO of olivine in the peridotites in
Cima di Gagnone in the presence of water. Tasaka et al. (2008)
reported water-induced Type-B CPO in highly depleted dunites
from the Imono peridotite body within the subduction-type
Sanbagawa metamorphic belt in southwest Japan. Jung (2009)
found both Type-B and Type-E CPOs of olivine in serpentinized
peridotites in Val Malenco, Italy. Skemer et al. (2013) reported
the water-induced Type-E CPO of olivine from Josephine
peridotites in southwest Oregon, in the United States. Michibayashi
and Oohara (2013) reported C- and E-type CPOs of olivine in a
hydrated ductile shear zone from the Fizh massif, Oman ophiolite.
Tab l e 3. Water-induced CPOs of olivine found in natural rocks
Fabric type Rock type Location Reference
B-type Dunite Higashiakaishiyama, SW Japan Mizukami et al. (2004)
Garnet peridotite Cima di Gagnone, Central Alps Skemer et al. (2006)
Dunite Southern Mariana Trench Michibayashi et al. (2007)
Depeleted dunite Snabagawa metamorphic belt, Japan Tasaka et al. (2008)
Serpentinized peridotite Val Malenco, Italy Jung (2009)
Mylonitic peridotite Bergen arc, Western Norway Jung et al. (2014b)
Spinel peridotite Shanwang, Eastern China Park & Jung (2015)
Chlorite peridotite Amklovdalen, WGR, Western Norway Kim & Jung (2015)
Mylonitic peridotite Navajo volcanic fiend, Colorado Plateau, USA Behr & Smith (2016)
Spinel lherzolitie El Aprisco, Calatrava volcanic field, Spain Puelles et al. (2016)
C-type Garnet peridotite Cima di Gagnone, Central Alps Frese et al. (2003)
Garnet peridotite Otroy Island, WGR, Western Norway Katayama et al. (2005)
Dunite Fizh massif, Oman ophiolite Michibayashi & Oohara (2013)
Garnet peridotite North Quidam UHP belt, NW China Jung et al. (2013)
Spinel peridotite Adam's Diggings, Rio Grande rift, USA Park et al. (2014)
Spinel lherzolitie El Aprisco, Calatrava volcanic field, Spain Puelles et al. (2016)
E-type Serpentinized peridotite Val Malenco, Italy Jung (2009)
Harzburgite Josephine peridotite, SW Oregon, USA Skemer et al. (2013)
Dunite Fizh massif, Oman ophiolite Michibayashi & Oohara (2013)
Mylonitic peridotite Bergen arc, Western Norway Jung et al. (2014b)
Spinel peridotite Shanwang, Eastern China Park & Jung (2015)
Chlorite peridotite Amklovdalen, WGR, Western Norway Kim & Jung (2015)
Spinel peridotite Yugu, South Korea Park & Jung (2017)
Mylonitic peridotite Ronda massif, Southern Spain Précigout et al. (2017)

992 Haemyeong Jung
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Jung et al. (2013) found water-induced strong Type-C CPOs in
ultra-high-pressure (UHP) garnet peridotites from the North
Qaidam UHP collision belt in northwest China. In that study
the olivine contained water up to C
OH
= 1,130 ± 50 ppm H/Si, the
highest water content in olivine with the Type-C CPO in natural rock.
Park et al. (2014) reported Type-C CPOs of olivine in the
mantle xenoliths from the Adam’s Diggings at a rift shoulder in
the Rio Grande rift in the US, where spinel peridotites showed
evidence of rock deformation under wet conditions. Jung et al.
(2014b) found Type-B and -E CPOs of olivine in the peridotite
mylonites under a wet environment in the Bergen arc in western
Norway. Park and Jung (2015) reported Type-B and -E CPOs of
olivine in the spinel peridotites from mantle xenoliths in Shanwang,
eastern China. Kim and Jung (2015) studied chlorite peridotites
from Amklovdalen in the western gneiss region in western Norway
and reported both Type-B and Type-E CPOs of olivine. Behr
and Smit h (2016) re ported Type-B C POs of olivine in t he mantle
xenoliths from a mantle wedge setting in the Navajo volcanic
field in the Four Corners region of the Colorado Plateau, the
US, confirming that this fabric does form in natural subduction
zones. Czertowicz et al. (2016) reported dislocation glide on E-
type slip system in the coarse pre-mylonitised grains of olivine
under hydrous condition in Anita shear zone in New Zealand,
probably within hydrated sub-arc mantle lithosphere. Puelles et
al. (2016) reported both Type-B and -C CPOs of olivine in the
mantle xenoliths in El Aprisco in the Calatrava volcanic field in
central Spain. Recent study on microstructures of Pinatubo
peridotite xenoliths Yamamoto et al. (2017) found some dislocations
with the (001)[100] slip system in olivine which could have
been formed by the deformation under moderate water content
and low-temperature conditions. Park and Jung (2017) recently
reported Type-E CPOs of olivine in the ultramylonites (Figs. 2e
and 7) from the Yugu peridotite body in Yugu, South Korea.
Precigout et al. (2017) also found Type-E CPOs of olivine in the
mylonitic peridotites in the Ronda massif, Southern Spain.
2.2. Effect of Temperature and Pressure on the
CPOs of Olivine
2.2.1. Effect of temperature on the CPOs of olivine
Katayama and Karato (2006) investigated the effect of temperature
on the CPO of olivine at P = 2 GPa and T = 1,000–1,100 °C.
Samples were deformed at the constant strain rates of 3.8 × 10
–4
–
3.2 × 10
–5
s
–1
under water-saturated conditions using the Griggs
apparatus. The Type-B CPO of olivine occurred at higher stresses
than the Type-C CPO. In addition, the stress magnitude at which
the Type-B to -C CPO transition occurs decreased significantly
with decreasing temperature.
2.2.2. Effect of pressure on the CPOs of olivine
Couvy et al. (2004) studied the effect of pressure on the CPO
of olivine, performing relaxation experiments on forsterite (Mg
2
SiO
4
)
aggregates using a multi-anvil apparatus at P = 11 GPa and T =
1,400 °C. In that study, shear strain was limited to γ = 0.2 because
of the conditions of the experimental facility, but a weak Type-C
CPO of olivine was observed, suggesting that high pressure
makes Type-C fabric. However, this result is associated with the
following uncertainties: (1) the analysis of water content of olivine
Fig. 7. Microstructural evolution and CPO evolution of olivine in the Yugu peridotites in Yugu, South Korea (Park and Jung, 2017). From proto-
mylonite (PM) via mylonite (M) to ultra-mylonite (UM), both shear strain and water activity are increased whereas recrystallized grain-size of
olivine is decreased. Crystal preferred orientations (CPOs) of olivine are changed with the textural types of peridotites, from A-type (PM) via
D-type (M) to E-type (UM).

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after the experiments using Fourier Transformation Infrared
(FTIR) spectroscopy revealed that the samples contained a large
amount of water (1,500–2,500 ppm H/Si). Deformation of olivine
in wet conditions (C
OH
≥700 ppm H/Si) can produce Type-C
CPO of olivine (Jung and Karato, 2001); (2) stress was varied
during the experiment from 100 to 1,500 MPa because of the
stress-relaxation experiment. High stress favors [001] slip in olivine
(Carter and Avé Lallemant, 1970) and can induce changes in
olivine fabric (Jung et al., 2006; Katayama and Karato, 2006); (3)
the sample of forsterite used contained no Fe in olivine, whereas
olivine in nature is Fe-bearing in the upper mantle (~10%); and
(4) the shear strain was so small (γ = 0.2) that it is not certain
that the CPO represents the real fabric of the Earth where shear
strain is considered large.
More experimental studies of olivine aggregates at high pressure
were performed by exercising great care on the water content,
stress, and shear strain and pressure was found to induce changes
in the olivine CPO from Type-A to Type-B above 3 GPa (Jung et
al., 2009b). Deformation experiments of natural olivine aggregates
((Mg
0.9
Fe
0.1
)
2
SiO
4
) were conducted using a modified Griggs
apparatus at P =2.5–3.6 GPa and T = 1,300°C under dry conditions
(C
OH
≤90 ppm H/Si) with a large shear strain (γ=3–6). Samples
were d eforme d at cons tant s trai n rate s (2 × 10
–4
–6 × 10
–5
s
–1
) and
the CPO of olivine was measured using the SEM/EBSD (scanning
electron microscope/electron backscattered diffraction) technique
at the Seoul National University in South Korea. Olivine Type-B
CPO was developed at the pressures of 3.1 GPa and 3.6 GPa and
the temperature of 1,300 °C whereas Type-A CPO was formed
at the low pressure of 2.5 GPa with other conditions similar to
the higher-pressure experiments (Fig. 8) (Jung et al., 2009b). The
pressure-induced Type-B CPO of olivine occurred at the pressure
greater than 3 GPa. A subsequent study on the deformation of
olivine aggregates using the D-Dia (deformation-dia), a multi-
anvil high-pressure apparatus, confirmed that similar Type-B
CPO of olivine was formed at 5 GPa (Ohuchi et al., 2011).
Recently, more experiments were performed on the deformation
of olivine aggregates at high pressure under wet and dry conditions
(Ohuchi and Irifune, 2013, 2014; Ohuchi et al., 2015). To
Fig. 8. Pole figures of olivine showing the effect of pressure on the CPO of olivine (after Jung et al., 2009b). Arrows show the shear sense,
and north-south poles correspond to the shear plane normal. Contours correspond to multiples of a uniform distribution of data points. In
all three specimens represented here, the water content was undetectable. (a) T = 1300 °C, γ = 3, differential stress = 120 MPa. (b) T = 1300 °C,
γ = 3, differential stress = 150 MPa. (c) T = 1300 °C, γ = 6, differential stress = 390 MPa. A half-width of 20° was used to draw the pole figures.
MPD = maximum pole figure density.

994 Haemyeong Jung
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compare the olivine CPOs in those studies, one needs to pay
attention to the measurement of olivine water content. The water
content of olivine (Jung and Karato, 2001; Jung et al., 2006) was
originally measured inside single crystal olivine without any
cracks, inclusions, or grain boundaries. Recently, Soustelle and
Manthilake (2017) deformed olivine-orthopyroxene aggregates
under simple shear at high pressures using the multi-anvil press
with shear strains of γ = 0.5–1.3. They found that the Type-B
CPO of oliv ine d evel oped at hig h pre ssure s of 3, 5 , and 8 GPa f or
olivine plus orthopyroxene content of 12.5% and 25% at the
temperatures of 1,300, 1,400, and 1,500 °C, respectively.
2.2.3. Natural example of pressure-induced CPOs of
olivine
Deformation fabrics of olivine from diamond-bearing garnet
peridotites in Finsch, South Africa were studied (Lee and Jung,
2015). They found strong Type-B CPOs of olivine in the samples
originated from a depth of 120 km (P = 4 GPa, T = 1,000 °C)
based on the analysis of the chemical composition of minerals
(thermobarometry data from the electron microprobe analysis)
and the existence of diamonds in garnet peridotites. Measurements
of the water content of both olivine and orthopyroxene using
FTIR spectroscopy revealed that both olivine and orthopyroxenes
are dry, indicating that strong Type-B CPOs of olivine were
formed under dry and high-pressure conditions. These observations
indicate that the strong Type-B CPOs in garnet peridotites of
Finsch, South Africa is the first natural example of pressure-induced
fabrics of olivine.
2.3. Effect of Large Shear Strain and Deformation
History on the CPOs of Olivine
2.3.1. Effect of large shear strain on the CPOs of olivine
The first shear deformation experiment of olivine aggregates
under dry conditions using the torsion apparatus for a large shear
strain (up to γ = 5) was conducted by Bystricky et al. (2000) at
the pressure of 300 MPa and 1,200 °C. They reported a Type-D
CPO of olivine at shear strains of γ = 2, 4, and 5. Later, Hansen et
al. (2012) deformed olivine aggregates (Fo
50
) for a large shear
strain (up to g ~10) using a torsion apparatus under dry conditions
at P = 250 MPa and 1200 °C. The Type-D CPO of olivine was
observed at a shear strain of γ ~3.5, but the Type-A CPO was
observed at a shear strain of γ ~10. To examine the systematics of
the evolution of olivine crystallographic fabrics at high strain,
Hansen et al. (2014) conducted more torsion experiments on olivine
aggregates (Fo
50
) under dry conditions at the pressures of 250
and 300 MPa and at 1200 °C with shear strains of up to γ ~19. A
steady-state fabric was not reached until the shear strain was
greater than 10. The authors showed that Type-D CPOs of olivine
developed with increasing strains up to γ = 9 and γ = 14, and
showe d Type-A CPOs at shear strains of γ = 7, 10, 11, and 19. These
results indicate that more study is probably needed to understand
the development of CPOs of olivine with large shear strain.
2.3.2. Effect of deformation history on the CPOs of
olivine
Recently, the effect of deformation history on the CPO of
olivine was studied by Boneh and Skemer (2014) using natural
samples of Åheim dunite that had a pre-existing CPO of olivine.
Deformation experiments were conducted using the Griggs
apparatus at 1 GPa and 1,200 °C with uniaxial strain (0.7). Samples
were deformed in three orientations, in which the shortening was
imposed perpendicular, oblique, and parallel to the pre-existing
foliation. The evolution of the CPO of olivine was distinct for
three initial orientations and none of the CPOs was observed to
reach steady state.
Numerical modeling studies on the olivine CPO development
were performed previously, producing a strong CPO of olivine
(Wenk and Tomé, 1999; Tommasi et al., 2000; Kaminski and
Ribe, 2001, 2002; Kaminski et al., 2004; Castelnau et al., 2008;
Castelnau et al., 2009; Castelnau et al., 2010). Recent numerical
studies on the development of olivine CPO using the dynamic
recrystallization-induced LPO (D-Rex) and the viscoplastic
self-consistent (VPSC) models (Boneh et al., 2015) identified
similar trends suggesting that a large strain is required to reach a
steady state CPO. In many cases, models initiated with a pre-
existing CPO require greater strain (about 3–5 times) to reach
steady state CPO than models initiated with a uniform CPO.
Signorelli and Tommasi (2015) modified a viscoplastic self-
consistent code to simulate the effects of subgrain rotation
recrystallization on the CPO of olivine. They found that the easy
slip system rotates fast towards parallelism with imposed shear
and that steady-state CPO (orientation and intensity) is reached
at shear strains of γ > 5.
2.4. CPOs of Olivine in Natural Shear Zones
CPOs of olivine in natural shear zones were studied in Josephine
Peridotite in southeastern Oregon, US (Warren et al., 2008;
Skemer et al., 2010; Hansen and Warren, 2015), in the Red Hills,
New Zealand (Webber et al., 2008), in the Hilti massif, Semail
ophiolite, Oman (Linckens et al., 2011), in an extensional shear
zone in the mantle, Lanzo massif, Italy (Kaczmarek and Tommasi,
2011), in an oblique-slip low-angle shear zone in the Beni Bousera
peridotite (Rif Belt, Morocco) (Frets et al., 2014), in the mylonitic
peridotites in the Ronda massif, Southern Spain (Precigout et
al., 2017), and in Yugu peridotites in South Korea (Fig. 7) (Park
and Jung, 2017). These studies suggested that the re-orientation

Crystal preferred orientations of olivine and hydrous minerals 995
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of olivine in rocks with pre-existing textures requires large
strains. For example, a shear strain of γ > 4 was needed to re-orient
the CPOs of olivine with respect to the shear zone kinematics
(Hansen and Warren, 2015).
2.5. Other Possibilities for the Formation of the CPOs
of Olivine
Experimental study at the pressure of 300 MPa and temperature
of 1200 °C (Holtzman et al., 2003) reported, in the presence of
melt, a Type-B like CPO of olivine which is characterized as a
strong concentration of [010] axes aligned subnormal to the
shear plane and a weak girdle of both [100] and [001] axes aligned
subparallel to the shear plane. However, this type of melt-induced
CPO of olivine has been rarely reported in natural rocks. There
is also a report of the development of CPO of iron-free olivine
(forsterite) which was experimentally produced during diffusion
creep at the temperature of 1,200–1,350 °C (Miyazaki et al., 2013).
Fabric analysis of olivine in spinel peridotite xenoliths of Jeju Island
in South Korea (Yang et al., 2010) showed a weak activation of {0kl}
[100] slip system in the porphyrocalstic and mylonitic peridotites.
The results of the trace element analysis in that study revealed
that the smaller the grain size and weaker the fabric, the more
enriched in LREE and HFSE are the peridotites, indicating a strong
relationship between metasomatic agents and mantle shear zones.
A weak Type-C CPO of olivine was reported in Xugo UHP
garnet peridotites from the southern Sulu UHP terrane in China
(Wang et al., 2013b). The Type-C CPO of olivine was generated
by a dominant dislocation-accommodated grain boundary sliding
(DisGBS) with a minor contribution from the diffusion creep at
elevated pressure. Nagaya et al. (2014) reported that the Type-B
CPO of olivine can form as a result of the static topotactic growth
of olivine after the high-temperature breakdown of foliated
serpentinite. Wang et al. (2013a) reported Type-B CPO of olivine
in dunite from Raudkleivane, Amklovdalen and Type–C CPO
of olivine in garnet harzburgite from Ugelvik, Otroy in Norway.
Based on low water content in olivine, they interpreted that those
CPOs were produced by high stress or high pressure. However,
there is a high possibility that water in olivine was lost during
exhumation process because of high diffusivity of hydrogen in
olivine (Mackwell and Kohlstedt, 1990).
The Type-B CPO of olivine was also reported in peridotites
from the Ronda massif in Spain (Precigout and Hirth, 2014). The
Type-B CPO was suggested to be resulted from the enhancement
of the grain boundary sliding (GBS) with decreasing grain size.
The effect of finite strain geometry on CPO of olivine was
investigated using naturally deformed mantle rocks (Chatzaras
et al., 2016). They showed that finite strain geometry controls
the development of axial-type olivine CPO; axial-[010] and axial-
[100] CPOs form in relation to oblate and prolate fabric ellipsoids,
respectively. Cao et al. (2017) reported CPOs of olivine similar
to Types C and B in Songshugou peridotites and suggested that
those CPOs were formed by a diffusion-accommodated grain
boundary sliding (DifGBS) at high temperatures.
2.6. Scaling to the Nature
Because some of the conditions in experimental studies (e.g.,
the strain-rates) are different from those in the Earth, we need to
understand the scaling law for fabric transitions if experimental
results were to be applied to the Earth. This issue was already
discussed in previous study (Jung et al., 2006) and is summarized
below. Any fabric transition occurs when the rates of two
processes (e.g., strain-rates of two slip systems) become similar.
Therefore a generic equation to define a fabric boundary is
A
1
(T, P, C
OH
, σ) = A
2
(T, P, C
OH
, σ), (1)
where A
1
and A
2
are the rates of processes responsible for a
fabric development (e.g., strain-rate), T is the temperature, P
is the pressure, C
OH
is the water content, and σ is the stress.
Therefore, the transition conditions between two types of fabric
are given by a hyper-surface defined as,
f (T, P, C
OH
, σ) = 0. (2)
In most cases, the rates of these processes can be given by a set
of non-dimensional variables as
,
(3)
and consequently
. (4)
Therefore, the boundaries between different types of CPO
can be given by a hyper-surface in a multi-dimensional space
that does not include strain-rate explicitly. Therefore, the
fabric boundaries do not explicitly depend on strain-rates so
that the fabric boundaries determined by laboratory experiments
can be applied to the Earth’s interior where deformation occurs
at much slower strain-rates. The only difference between
laboratory and Earth is that because laboratory experiments
are conducted at much faster strain-rates than those in Earth,
laboratory studies can explore only limited range of parameter
space (e.g., relatively high stress regions).
3. CPOs OF ORTHOPYROXENE
Orthopyroxene is the second dominant mineral in the upper
A
1
′T
T
m
P()
-------------- C
OH
σ
μPT,()
-----------------,,
⎝⎠
⎛⎞
A
2
′T
T
m
P()
-------------- C
OH
σ
μPT,()
-----------------,,
⎝⎠
⎛⎞
=
f′T
T
m
P()
-------------- C
OH
σ
μPT,()
-----------------,,
⎝⎠
⎛⎞
0=

996 Haemyeong Jung
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mantle and constitutes most of the upper mantle along with
olivine (Ringwood, 1970). To better understand the seismic
anisotropy in the upper mantle, one needs to understand the
CPO of orthopyroxene as well (Jung et al., 2010). However,
experimental studies on the CPO of orthopyroxene are very
limited. According to a review on the CPOs of orthopyroxene in
natural mantle rocks (Christensen and Lundquist, 1982), the
CPO of orthopyroxene is characteriz ed as [100] axes al igned normal
to foliation and [001] axes aligned parallel to the lineation,
indicating a major slip system of (100)[001]. This type of
orthopyroxene CPO was classified and defined as Type-AC CPO
(Fig. 9) (Jung et al., 2010), which has been the most commonly
observed CPO in natural rocks (Ishii and Sawaguchi, 2002;
Skemer et al., 2006; Xu et al., 2006; Hidas et al., 2007; Tommasi
et al., 2008; Soustelle et al., 2009; Jung et al., 2010; Puelles et al.,
2012). There are three other types of orthopyroxene CPOs
found in the study of mantle xenoliths in the Spitsbergen, Svalbard
in the Arctic (Jung et al., 2010). Figure 9 shows the Type-AC
CPO of orthopyroxene as well as three others (Type-AB, -BC,
and -ABC) (Jung et al., 2010). The Type-AB CPO of orthopyroxe ne
was defined as [100] axes aligned subnormal to the foliation and
[010] axes aligned subparallel to the lineation. The Type-BC CPO
of orthopyroxene was defined as [010] axes aligned subnormal
to the foliation and [001] axes aligned as subparallel to the lineation.
The Type-ABC CPO of orthopyroxene was defined as both [100]
and [010] axes aligned as a girdle subnormal to the lineation
and [001] axes aligned subparallel to the lineation. The reason
for the occurrence of different CPO types of orthopyroxene was
considered to be a modal proportion of orthopyroxene in the
sample (Jung et al., 2010), but it is still not clearly understood.
Effects of Al and water on the CPO of MgSiO
3
enstatite,
anhydrous and hydrous aluminous enstatite had been investigated
at the pressure of 1.5 GPa and temperature of 1,100 °C using D-
Dia apparatus (Manthilake et al., 2013). In MgSiO
3
enstatite and
hydrous aluminous enstatite, dislocations showing (100)[001]
slip systems (i.e., Type-AC CPO) was observed. However, EBSD
analysis of anhydrous aluminous enstatite indicated operation
of (010)[001] slip system which produces Type-BC CPO. There
are two other experimental studies on the deformation of two-
phase mixtures of orthopyroxene and olivine. Sundberg and
Cooper (2008) conducted deformation experiments of samples
at 1.6 GPa and 1,200 °C, using the Griggs apparatus, and reported
that orthopyroxene shows Type-AC CPO (Fig. 9) for samples
with an olivine:orthopyroxene ratio of (35:65%). Recently, at
Fig. 9. Representative pole figures of
orthopyroxene (opx: enstatite). Four
types of CPOs of orthopyroxene are
shown after Jung et al. (2010). Pole fig-
ures of the crystallographic orientation
of enstatite are presented in the upper
hemisphere using an equal area projec-
tion. The color coding refers to the den-
sity of data points (the numbers in the
legend correspond to the multiples of
uniform distribution). Type-AB: sample
SVF-04, N = 172. Type-AC: sample SVF-
49, N = 176. Type-BC: sample SVF-30, N
= 138. Type-ABC: sample SVF-71, N =
168. A half scatter width of 30° was
used. S: foliation, L: lineation.

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high pressures of 3, 5, and 8 GPa and high temperatures of
1,300, 1,400, and 1,500 °C, respectively, Soutelle and Manthilake
(2017) deformed samples (a mixture of olivine and orthopyroxene)
using D-Dia at shear strains of 0.5–1.3. They found that CPOs
of orthopyroxenes are ABC-type (Jung et al., 2010) for samples
with olivine:orthopyroxene ratios of (50:50%), characterized as
[001] axes aligned subparallel to the shear direction and both
[100] and [010] axes aligned subnormal to the shear direction.
4. CPOs OF SERPENTINE (ANTIGORITE)
To understand the CPO development of serpentine, deformation
experiments were conducted on serpentinite under simple shear
at the high pressure of 1 GPa and temperatures of 300 and 400 °C
using a Griggs apparatus (Katayama et al., 2009). The sample
was serpentinite consisting mostly of antigorite. The authors found
that the antigorite CPO was characterized as [001] axes aligned
subnormal to the shear plane and [100] axes aligned subparallel
to the shear direction. Similar CPOs of serpentine were observed in
few natural samples (Bezacier et al., 2010; Brownlee et al., 2013).
On the other hand, CPOs of serpentine (antigorite) in natural
rock were investigated using serpentinites from Val Malenco and
Punta Bettolina in northwest Italy (Jung, 2011). The amount of
serpentine in the samples varied between 40% and 93%. The
CPO of antigorite is characterized as [001] axes aligned subnorma l
to the foliation but [010] axes aligned subparallel to the lineation
(Figs. 10a–c), consistent with other observations of the CPOs of
antigorite in many natural rocks (Hirauchi et al., 2010; Soda and
Takagi, 2010; Nishii et al., 2011; Brownlee et al., 2013; Nagaya et
al., 2014; Watanabe et al., 2014). However, for reasons that are
not yet understood, the alignment of [010] axes subparallel to the
lineation is different from the CPO produced by an experimental
study (Katayama et al., 2009).
5. CPOs OF CHLORITE
Deformation fabrics of chlorite were studied by Kim and Jung
(2015) using chlorite peridotites in Amklovdalen, Western Gneiss
Fig. 10. Typical CPOs of serpentine
(antigorite) in serpentinites from Val
Malenco (a and b) and Punta Bettolina
(c and d), northern Italy (Jung, 2011). (a)
Sample VM1 consists of Ant: 40%, Ol:
52%, Di: 5%, and Mgt: 3% where Ant:
antigorite, Ol: olivine, Di: diopside, and
Mgt: magnetite. (b) Sample VM3 con-
sists of Ant: 87%, Ol: 8%, and Mgt: 5%.
(c) Sample 12B consists of Ant: 93%, Ol:
5%, and Mgt: 2%. (d) Sample 12M con-
sists of Ant: 78%, Ol: 4%, and Mgt: 18%.
Pole figures of serpentine are presented
in equal-area and lower-hemisphere
projections. The E-W direction corresponds
to lineation (x). The N-S direction (z) rep-
resents the direction normal to foliation.
The color coding represents the density
of the data points. The contours corre-
spond to multiples of a uniform distri-
bution. A half-width of 30° was used to
draw the pole figures. n: number of
grains analyzed.

998 Haemyeong Jung
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Region (WGR) in southwest Norway. Two types of chlorite
CPOs (Type-1 and -2) were found. Figure 11a shows that
chlorite [001] axes are strongly aligned subnormal to foliation and
both [100] axes and (010) poles subparallel to foliation. This
type of CPO is defined as the Type-1 CPO of chlorite (Kim and
Jung, 2015). Figure 11b shows that chlorite [001] axes are aligned
as a girdle subnormal to the lineation. This type of CPO is defined
as the Type-2 CPO of chlorite. Type-1 CPO of chlorite was also
observed in natural rocks (Puelles et al., 2012; Morales et al.,
2013; Padrón-Navarta et al., 2015; Kang and Jung, submitted).
Type-2 CPO of chlorite was less commonly observed and reported
in natural samples (Padrón-Navarta et al., 2015; Wallis et al.,
2015). The reason for the occurrence of these two chlorite CPO
types is currently unknown, and may be a topic of further research.
6. CPOs OF AMPHIBOLE (HORNBLENDE)
6.1. CPOs of Amphibole Experimentally Produced
at High Pressure and Temperature
To understand the CPO development of the amphibole,
deformati on experiments on amphibole (hornbl ende) in amphibo lit e
were conducted under simple shear at the high pressure of
1 GPa and temperatures of 480, 500, 600, 700 °C using the
modified Griggs apparatus (Fig. 4b) (Ko and Jung, 2015). The
sample was natural amphibolite consisting mainly of hornblende,
plagioclase, and minor ilmenite (Fig. 2f). Ko and Jung found
three types of amphibole (hornblende) CPOs (Fig. 12a) depending
on temperature and stress (Fig. 12b). Type-I CPO of amphibole
was found at low temperatures and varied stress conditions. It
was characterized as [001] axes aligned subparallel to the shear
direction and (100) poles aligned subnormal to the shear plane.
Type-II CPO of amphibole was found at an intermediate
temperature range (550–700 °C) and high-stress conditions,
and characterized as (010) poles aligned subparallel to the shear
direction and (100) poles aligned subnormal to the shear plane.
Type-III CPO of amphibole was found at high temperature,
low-stress conditions and characterized as both (010) poles and
[001] axes aligned subparallel to the shear plane and (100) poles
aligned subnormal to the shear plane (Fig. 12).
In a study of amphibole fabric formation during diffusion
creep (Getsinger and Hirth, 2014), basalt powder was used as the
starting material to which water was added to produce fine-grained
amphiboles. Shear deformation experiments were conducted at
the pressure of 1 GPa and high temperature of 800 °C. The CPO
of amphibole was characterized as [001] axes aligned subparallel
to the shear direction and [100] axes aligned subnormal to the
shear plane, which is a Type-I CPO (Fig. 12) (Ko and Jung, 2015).
6.2. CPOs of Amphibole found in Natural Rocks
Early studies of the CPO of hornblende were conducted
by Schwerdtner (1964) and Mainprice and Nicolas (1989).
Amphibole with Type-I CPO was found in many places in the
world: lower crustal rocks from the Ivrea Zone, Italy (Barruol and
Kern, 1996), Bergell tonalite in the Central Alps (Berger and
Stünitz, 1996), amphibolite mylonites from the Diancang Shan
in southwest Yunnan, China (Cao et al., 2010), metabasites from
the Aracena metamorphic belt in southwest Spain (Díaz Aspiroz
et al., 2007), the Lewisian in northwest Scotland, a classic tonalitic–
trondjhemite–granodioritic (TTG) gneiss complex (Tatham et al.,
2008), amphibolites from the East Athabasca mylonite triangle
in Saskatchewan, Canada (Ji et al., 2013), and in hornblende schist
(Ji et al., 2015). Recent study of amphibole fabric in hydrated
peridotites from Bjorkedalen, SW Norway also showed the
Type-I CPO of amphibole (Kang and Jung, submitted).
Type-II CPO of amphibole was found in amphibolite mylonites
from the Diancang Shan in southwest Yunnan, China (Cao et
al., 2010) and in amphibolite in Yeoncheon, South Korea (Jung
et al., 2014a). Type-III CPO of amphibole was reported in the
Acebuches metabasites in southwestern Spain (Díaz Aspiroz et
al., 2007), fine-grained amphibolite from the East Athabasca
Fig. 11. Typical CPOs of chlorite pre-
sented in the lower hemisphere using
an equal-area projection (modified from
Kim and Jung, 2015). (a) Type-1 CPO of
chlorite. Sample 436, N = 302. (b) Type-
2 CPO of chlorite. Sample 438, N = 395.
N represents the number of grains. The
white line (S) indicates the foliation and
the red dot (L) indicates the lineation. A
half-scatter width of 20° was used for
the contours. The red color represents
the high density of data points, and the
numbers in the legend correspond to
the multiples of uniform distribution.

Crystal preferred orientations of olivine and hydrous minerals 999
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mylonite triangle in Saskatchewan, Canada (Ji et al., 2013), and
quartz-hornblende-biotite schist (Ji et al., 2015). Type-IV CPO
is defined as amphibole [001] axes aligned subparallel to the
lineation and both (100) and (110) poles aligned as a girdle
subnormal to the lineation. This type of CPO of amphibole was
reported in amphibolites from the Ryoke metamorphic belt in
southwest Japan (Imon et al., 2004), metabasites from the Aracena
metamorphic belt in southwest Spain (Díaz Aspiroz et al., 2007),
Fig. 12. Pole figures and fabric diagram of amphibole (hornblende). (a) Pole figures of three types of CPOs of the deformed hornblende in
simple shear at high pressure and high temperature conditions and (b) their fabric diagram (Ko and Jung, 2015). The x and z direction cor-
respond to the shear direction and the shear plane normal, respectively. The arrows indicate the sense of shear. The pole figures are pre-
sented in equal-area and lower-hemisphere projection with a half-width of 20°. The contours indicate the m.u.d. for the density of poles.
(Type-I) Sample JH54, P = 1 GPa, T = 480 °C, n = 202. (Type-II) Sample JH46, P = 1 GPa, T = 600 °C, n = 206. (Type-III) Sample JH74, P = 1
GPa, T = 640 °C, n = 216. n: number of measured grains. Differential stress: peak value of differential stress after yielding.

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the Lewisian of northwest Scotland (Tatham et al., 2008),
amphibolites in Cabo Ortegal, Spain (Llana-Fúnez and Brown,
2012), retrogressed Limo harzburgites, Limo massif, Cabo Ortegal
in northwest Spain (Puelles et al., 2012), and fine-grained amphibolite
and clinopyroxene amphibolite from the East Athabasca mylonite
triangle in Saskatchewan, Canada (Ji et al., 2013).
7. GEOPHYSICAL IMPLICATIONS
Only Type-A CPO of olivine had been used to interpret
seismic anisotropy observed in the upper mantle before the
paper (Jung and Karato, 2001) was published (Mercier, 1985;
Nicolas and Christensen, 1987; Silver, 1996; Savage, 1999;
Fig. 13. Seismic anisotropy of olivine for
different types of CPOs of olivine in Fig-
ure 6a (modified after Jung et al., 2006).
Seismic anisotropy is shown on a ste-
reographic projection in which the cen-
ter of a plot is the direction normal to
the shear plane, and the E-W direction
corresponds to the shear direction.
P-wave anisotropy, the amplitude of
shear wave splitting (dVs) and the direc-
tion of polarization of the faster shear
wave (Vs1) are shown.

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Mainprice et al., 2000; Smith et al., 2001) because no other types
of olivine CPOs were known at that time. However, there were
difficulties in explaining seismic anisotropies observed in
collision zones and hotspot regions such as Hawaii using the
Type-A CPO of olivine (Jung and Karato, 2001; Park and Levin,
2002). The seismic velocities and anisotropies of different types
of olivine CPOs are shown in Figure 13. Type-B, -C, -D, -E CPOs
of olivine produce different seismic signatures from Type-A
CPO (Fig. 13) (see also Jung et al., 2006; Karato et al., 2008). The
water content of olivine in the mid-ocean ridge basalt (MORB),
originating from the oceanic asthenosphere, was reported as
500–1,000 ppm H/Si (Hirth and Kohlstedt, 1996). In addition, a
higher water content exists in basalt originating from hotspots
(Wallace, 1998; Jamtveit et al., 2001). Therefore, the anomalous
seismic anisotropy observed below hotspots (Montagner and
Guillot, 2000; Gaherty, 2001), can be explained by water-induced
Type-C CPO of olivine. Seismic anisotropies produced by the
four orthopyroxene CPOs are shown in Figure 14; their seismic
signatures are also different (Jung et al., 2010). The seismic
properties of orthopyroxene should be carefully considered to
better understand the overall seismic anisotropy in subduction
zones.
Seismic anisotropy of the P- and S-wave was observed in the
mantle wedge in many subduction zones worldwide (i.e., Fig. 1)
(Savage, 1999; Park and Levin, 2002; Long and Silver, 2008;
Long, 2013; Long and Wirth, 2013; Wang and Zhao, 2013; Zhao
et al., 2016). Trench-parallel seismic anisotropy of the fast S-
wave was observed in many fore-arc areas and sub-slabs in
subduction zones (Ando et al., 1983; Fouch and Fischer, 1996;
Margheriti et al., 1996; Smith et al., 2001; Nakajima and Hasegawa,
2004; Long and van der Hilst, 2005; Abt et al., 2010; Long and
Becker, 2010; Di Leo et al., 2012; Long and Wirth, 2013; Wagner
Fig. 14. Seismic anisotropy of orthopy-
roxene for different types of CPOs of
orthopyroxene in Figure 9 (after Jung et
al., 2010). The east-west direction corre-
sponds to the lineation (L), and the
north-south corresponds to the folia-
tion normal. Azimuthal anisotropy of P-
waves (Vp) and polarization anisotropy
of S-waves are shown (AVs is a contour
plot of the magnitude of shear wave
polarization anisotropy and Vs1 is a plot
of the polarization direction of fast S-
waves along different orientations of
propagation).

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et al., 2013; Lynner and Long, 2014). The source of this trench-
parallel seismic anisotropy was proposed as: (1) the trench-
parallel mantle flow due to trench-roll back (Russo and Silver,
1994; Long and Silver, 2008; Long and Silver, 2009); (2) Type-B
CPO of olivine (Jung and Karato, 2001; Kneller et al., 2005; Jung
et al., 2006; Katayama and Karato, 2006; Kneller and van Keken,
2007; Karato et al., 2008); (3) the 3-D mantle flow around the
slab (Faccenda and Capitanio, 2012, 2013; Li et al., 2014; Lynner
Fig. 15. Seismic anisotropy of serpentine which was calculated from the CPOs of serpentine in Figure 10. The effects of the degree of ser-
pentinization and composition on seismic anisotropy are shown in equal-area and lower hemisphere projections (from Jung, 2011). The seis-
mic anisotropy of serpentine in all the samples is shown in the horizontal flow, where the Y and Z axes are rotated 90° relative to Figure 10.
The X-direction corresponds to the direction of lineation (flow direction). The Z-direction represents the direction normal to foliation (flow
plane). The compressional-wave velocity (Vp) and shear-wave anisotropy (AVs) are shown. Vs1 is a plot of the polarization direction of fast
S-waves along different orientations of propagation. The center of the stereonet corresponds to vertical propagation. For the vertical prop-
agation of S-waves, the polarization direction of fast S-waves is nearly perpendicular to the flow direction (lineation). Ant: antigorite, Mgt:
magnetite.

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et al., 2017); (4) fault or crack-induced anisotropy in the slab
(Faccenda et al., 2008; Healy et al., 2009); (5) strong radial
anisotropy (Song and Kawakatsu, 2012, 2013); (6) CPO of
serpentine in the slab-mantle interface and in the mantle wedge
(Katayama et al., 2009; Jung, 2011; Nagaya et al., 2016); and (7)
CPOs of chlorite (Kim and Jung, 2015; Kang and Jung, submitted)
and amphibole in the lower part of mantle wedge (Ko and Jung,
2015; Kang and Jung, submitted). Since olivine in the mantle
wedge is hydrated by the fluids from the dehydration of minerals
in the subducting slab (Peacock and Hyndman, 1999; van Keken
et al., 2011), and the stress is high in a collision zone in the
subduction zones, it is highly likely that Type-B CPO of olivine
is formed in the mantle wedge. This hypothesis is supported by
numerical modeling studies of the effect of Type-B olivine CPO
on seismic anisotropy in the subduction zone (Kneller et al.,
2005, 2007). It is also supported by many observations of Type-
B olivine CPOs in mantle xenoliths (Park and Jung, 2015) and
peridotites in subduction zone settings (Table 3) (Mizukami et al.,
2004; Skemer et al., 2006; Tasaka et al., 2008; Jung, 2009; Jung et
al., 2014b; Kim and Jung, 2015; Behr and Smith, 2016).
It is interesting to see the changes in seismic anisotropy patterns;
from trench-parallel S-wave anisotropy in the fore-arc area to
the trench-normal S-wave anisotropy in the back-arc area (Smith
et al., 2001; Nakajima and Hasegawa, 2004; Long and van der
Hilst, 2006; Long and Wirth, 2013). This pattern of seismic
anisotropy may be explained by the change in olivine CPO from
Type-B in the fore-arc to Type-A, -C (or -E) in the back-arc
(Kneller et al., 2005; Katayama and Karato, 2006; Kneller et al.,
2007; Karato et al., 2008; Jung, 2012). The trench-parallel seismic
anisotropy was also observed in the subducting slab and below
the slab at a depth greater than 100 km in the subduction zone
(Russo and Silver, 1994; Müller et al., 2008; Long and Silver,
2009; Abt et al., 2010; Di Leo et al., 2014; Lynner and Long, 2014;
Lynner et al., 2017). Because of the relatively dry conditions
below the slab (Karato et al., 2008), one possible explanation of
this seismic anisotropy is the Type-B olivine CPO that can be
produced by high pressure in dry conditions (Jung et al., 2009b;
Ohuchi et al., 2011; Soustelle and Manthilake, 2017). This is
supported by a recent study on Type-B olivine CPOs found in
diamond-bearing peridotites in Finsch, South Africa (Lee and
Jung, 2015), which is the first report of a natural example of
pressure-induced Type-B CPO of olivine.
In addition, anomalously long delay times (1–4 s) of S-waves
and strong trench-parallel anisotropy have been observed in
some subduction zones such as in the Ryukyu, Izu-Bonin, and
Tonga-Kermadec arcs (Smith et al., 2001; Anglin and Fouch,
2005; Long and van der Hilst, 2005; Greve et al., 2008). This
strong seismic anisotropy may be caused by the strong CPOs of
hydrous minerals in the lower part of the mantle wedge and at
the interface between slab and mantle wedge. Hydrous minerals
Fig. 16. Schematic diagram showing
the effect of the dipping angle of the
slab on the seismic anisotropy caused
by the CPO of chlorite (Fig. 11a), assum-
ing 2-D corner flow (from Kim and Jung,
2015). (a) Trench-normal seismic anisot-
ropy in the low-angle subduction zone
(θ ≤ 45°). (b) Trench-parallel seismic
anisotropy in the high-angle subduc-
tion zone (θ > 50°). (c) Change in the
seismic anisotropy corresponding to
the change in the dipping angle of the
slab. Blue and red bars represent
trench-normal and trench-parallel seis-
mic anisotropy of the fast S-wave,
respectively. (a) Low-angle (warm) sub-
duction zone. (b) High-angle (cold) sub-
duction zone. (c) Angle-changing
subduction zone.

1004 Haemyeong Jung
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such as serpentine, chlorite, and amphibole can be stable at high
pressure and temperature conditions down to ~200 km (Ulmer
and Trommsdorff, 1995; Pawley, 2003; Fumagalli and Poli, 2005).
Shear deformation experiments of those hydrous minerals
produce strong CPOs at high pressures (Katayama et al., 2009;
Ko and Jung, 2015). Recent studies on the deformation fabrics
of hydrous minerals (serpentine, chlorite, and amphibole) also
showed that strong CPOs of the hydrous minerals in natural rocks
are formed (Figs. 10 and 11) and the CPOs of those serpentine,
chlorite, and ampibole can produce a strong trench-parallel
seismic anisotropy (Figs. 15, 16, and 17b) (Jung, 2011; Kim and
Jung, 2015; Ko and Jung, 2015; Kang and Jung, submitted) and
long delay times of S-waves (Fig. 18). The seismic velocity and
anisotropy pattern of serpentine, chlorite, and amphibole were
investigated in detail (Figs. 15–17), revealing that the strong
trench-parallel seismic anisotropy in the slab and at the slab-
mantle interface where the hydrous minerals are stable can be
explained by the CPOs of the hydrous minerals when the
subduction angle of the slab is high (θ≥45°) (Jung, 2011; Kim
and Jung, 2015; Ko and Jung, 2015). Figure 18 shows the thickness
(L) of the anisotropic layer (i.e., antigorite, chlorite, hornblende,
and olivine) that explains a wide range of delay times (dt) of S-
waves. The figure shows that long delay times (large seismic
anisotropy) of S-waves in some subduction zones can be explained
by a thin anisotropic layer of hydrous minerals such as chlorite,
antigorite, and hornblende.
Fig. 17. Seismic signatures from three different CPO types of amphibole are shown in (a) continental crust and (b) subduction zone (from
Ko and Jung, 2015). (a) For horizontal flow in the continental crust, the anisotropy contours of the S-waves (AVs) show that the orientation
of high anisotropy depends on the CPO types of amphibole. (b) For the flow dipping at 45° in the subduction zone, seismic anisotropy is
strong, and the Vs1 polarization direction (blue bar) is parallel to the trench for all three CPO types of amphibole for a vertically propagating
S-wave (SKS). The blue and red bars indicate the polarization directions of the fast shear wave (Vs1) and slow shear wave (Vs2), respectively.
Hb, hornblende.
Fig. 18. A diagram showing the relationship between delay time (dt)
and anisotropic layer thickness (L) of individual mineral. The follow-
ing equation (Silver and Chan, 1991; Mainprice and Silver, 1993) was
used: dt/L = AVs/<Vs>, where dt is the delay time of the shear waves,
AVs is the anisotropy of the S-wave for a specific propagation direc-
tion, and <Vs> is the average velocity of the fast and slow S-wave
velocities. To calculate delay time, seismic anisotropy data of olivine
(sample JK8; AVs = 5%) (Jung and Karato, 2001), antigorite (sample
VM3; AVs = 34%) (Jung, 2011), antigorite (sample HKB-B; AVs = 24%)
(Watanabe et al., 2014), chlorite (sample 1194-2; AVs = 46%) (Kang
and Jung, submitted), and hornblende (sample JH65; AVs = 12%) (Ko
and Jung, 2015) were used.

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A part of seismic anisotropy in subduction zones can be
attributed to the other hydrous minerals such as glaucophane,
lawsonite, and epidote in subducting slabs. There are some
previous reports on the study of CPO and resultant seismic
anisotropy of glaucophane (Cao et al., 2013; Kim et al., 2013; Cao
and Jung, 2016), lawsonite (Kim et al., 2013, 2016; Cao et al.,
2014; Cao and Jung, 2016), and epidote (Cao et al., 2011, 2013).
However, these data are very limited so far and more detail studies
on the development of CPOs of those minerals and resultant
seismic signatures are needed to better understand the seismic
anisotropy in the subducting slabs.
8. CONCLUSIONS
Crystal preferred orientations (CPOs) of olivine, orthopyroxene,
serpentine, chlorite, and amphibole in previous experimental
research and in natural rocks were reviewed, and the seismic
anisotropies of those minerals were discussed. Water-induced
CPOs of olivine, such as Type-B, -C, and -E found in experimental
studies, were also observed in many natural rocks and could be
very important for interpreting seismic anisotropies in the upper
mantle. Hydrous minerals such as amphibole, chlorite, and
serpentine in the lower part of the mantle wedge and at the slab-
mantle interface can also produce strong CPOs, which can be
used to interpret anomalously strong seismic anisotropies in
some subduction zones. In the future, hydrous minerals in the
subducting slab (i.e., glaucophane, epidote, and lawsonite)
should be investigated in detail to better understand the seismic
anisotropy in the slab in subduction zones.
ACKNOWLEDGMENTS
H.J. would like to thank colleagues at the Tectonophysics
Laboratory at the Seoul National University and other institutions
for their help in various projects. H.J. wishes to thank Y. Park
and S. Jung for preparing Tables and S. Choi for his help in
preparing Figure 3. H.J. would also like to express sincere gratitude
to Dr. Simon Wallis and an anonymous reviewer for their valuable
comments and suggestions. This study was supported by the NRF
grant of Korea (NRF-2017R1A2B2004688) and by KMIPA2017-
9020.
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