The Second Myanmar National Conference on Earth Sciences (MNCES, 2018) 113
November 29-30, 2018, Hinthada University, Hinthada, Myanmar
Department of Geology, Monywa University, Monywa, Sagaing Region, Myanmar
Petrogenesis of Metapelitic Rocks Exposed in Ka Ka-Naung Pein-
Man Hlwe Area, Katha Township, Sagaing Region
Aung Khin Soe
Abstract
The study area lies in Katha Township, northeastern part of Sagaing Region. It is situated between Latitude 24° 17′ to 24° 25′ N and Longitude 96° 16′ to 96° 24′ E. The presence of the
distinctive mineral assemblages such as chlorite-muscovite-quartz, biotite-muscovite-chlorite-
quartz and garnet-muscovite-biotite-quartz in metapelite point out that the study area falls
within the lower greenschist facies to amphibolites facies. Some textural features and
lithologic characters indicate that the metamorphic rocks of the Katha-Gangaw Range of the
study area may probably be metamorphosed from the mixture of pelitic and psammitic rocks
with subordinate amount of basic rocks of Late Jurassic to Early Cretaceous age. Three
metamorphic zones such as chlorite, biotite and garnet zones are recognized. Although
equilibrium is difficult to attain and P-T conditions are not certain, the chlorite zone is to be in
the 350 to 450°C range. The equilibrium conditions of biotite zone are 420°C at about 0.35
GPa. The porphyroblasts of almadine garnets do not occur until the temperature of 460-500°C
in typical pelites and the metamorphic grade starts to enter the lower amphibolites facies. There is neither precise time of metamorphism nor available radiometric dating for the
metamorphic rocks of the study area. The time of metamorphism of the present study area can
be ascertained with the neighbouring area and some establish area especially on the basis of
lithologic similarity and lateral continuity. So, the time of metamorphism of the Katha-
Gangaw Range (including study area) could be assigned tentatively to Late Cretaceous to
Early Oligocene. The sequence of metamorphic conditions encountered could be compared to
the medium P/T (intermediate pressure and intermediate temperature) facies series of
Barrovian Type.
Keywords: pelitic and psammitic rocks, equilibrium, Barrovian Type
Introduction
The study area lies in Katha Township, northeastern part of Sagaing Region. It is
situated between Latitude 24° 17ʹ to 24° 25ʹ N and Longitude 96° 16ʹ to 96° 24ʹ E of
UTM map sheet No. 2496 07. It can readily be approached by car and by ship from
Mandalay, Katha and Banmaw throughout the year. The location map of the study area is
shown in (Fig.1). The main ridge comprises in the study area is east of Katha-Gangaw Range.
Although there are some previous geologic accounts on the study area, petrogenesis of
metamorphic rocks and progressive metamorphism deduced from mineral isograds on
metamorphic rocks have not been documented yet. Thus, I was carried out this present
research work.
Regional Geologic Setting
Mitchell (1981) divided the Myanmar region into four plates, viz., (1) Indian Plate
lying west of the Indo-Burman Ranges; (2) The Eastern Burma Plate extending from the
Indo-Burman Ranges to the Sagaing-Namyin Fault; (3) The Shillong Plate lying north of the
Naga Hills and (4) The Asian Plate lying east of the Sagaing-NamyinFault.The study area lies
within the northern part of Central Cenozoic Belt (Central Lowland) and it is located in the
west of the western margin of Sino-Myanmar Ranges (Kachin-Shan-Tanintharyi Highlands
or Eastern Highlands) (Bender, 1983).According to Mitchell (1981)’s divisions, the study
area falls in the eastern part of Eastern Burma Plate and western part of Asian Plate. The
Sagaing Fault passes through the western part of this area.
114 The Second Myanmar National Conference on Earth Sciences (MNCES, 2018)
November 29-30, 2018, Hinthada University, Hinthada, Myanmar
Wuntho-Banmauk uplift (United Nations, 1978) is situated in the western part of the
area and it comprises chlorite, actinolite and mica schists and phyllites overlain by the
Mawgyi basalt (early Cretaceous), pillow lavas and volcaniclastics beneath Upper Albian
limestone. Pre-Albian rocks are intruded by andesite sills, by the early Upper Cretaceous
granodioritic Kanza Chaung Batholith, and by Tertiary minor intrusions. Post-Oligocene,
Miocene sediments and some carbonate rocks are exposed between this uplift and Sagaing
Fault. The Katha-Gangaw Range is made up of pelitic metamorphic rocks and the first defile
of Ayeyarwady lies between the Katha-Gangaw Range and Tagaung-Myitkyina Belt
including Tagaung Taung Ultrabasic rocks (Cretaceous) (Aung Kyaw Thin, 2006).
The southern part of the study area is covered by Pleistocene gravels, Irrawaddy
Formation and Pondaung Formation (Myint Thein, et.al., 1982), Cenozoic volcanic and
ultrabasic volcanic rocks (serpentinite), Mayathein complex (schist, gneiss, marble and
migmatites), Katha Methamorphics (phyllite, talc schist, green schist, garnet-mica schist,
quartz-mica schist and amphibolites), Ngapyawdaw Chaung Formation (Triassic) (Myint
Thein et.al., 1982; L.Laja,1983), (Late Jurassic-early Cretaceous) (Maung Maung et.al.,2006)
and Wabo Chaung Formation (Oligocene) (DGSE,1976 in Nyan Win, 2008).
Jade Mines Belt, northern part of the area, is consisting of hornblende schist,
glaucophane schist, chlorite schist, kyanite schist and graphite schist (Chhibber, 1934). The
metamorphic rocks are generally trending NE-SW. The regional geologic setting of the study
area and its environs are shown in (Fig.2).
LEGEND
Figure (1). Location map of the study area
Study area
95°50ʹ 96°15ʹ 96°40ʹ
95°50ʹ
24°
0ʹ
96°15ʹ 96°40ʹ
24°
20
ʹ
24°
40
ʹ
24°
40
ʹ
24°
20
ʹ
24°
0ʹ
N
0 28 km
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November 29-30, 2018, Hinthada University, Hinthada, Myanmar
Figure (2). Regional geologic setting of the study area and its environs. (Source: MGS, 2014)
Study area
116 The Second Myanmar National Conference on Earth Sciences (MNCES, 2018)
November 29-30, 2018, Hinthada University, Hinthada, Myanmar
Distribution of Rock Units
The present study area is made up chiefly of metamorphic rocks. The metamorphic
rocks are of Late Jurassic -Early Cretaceous Katha Metamorphics rock units. They occupy
the entire bulk of the east of Katha-Gangaw Range and the metamorphic rocks are low to
medium grade. It is noteworthy that the metamorphic units pass into one another in a
gradational manner. The Katha Metamorphics rock units cover two-third of the study area.
The Katha Metamorphics are subdivided into three informal units: lower Unit I,
middle Unit II and upper Unit III. Based on the minerals, mineral assemblages and
lithologies, the units are arranged in orderly. The lower Unit I is chiefly composed of garnet
biotite schist, garnet muscovite schist and garnet quartzite. The middle Unit II is essentially
composed of sericite schist, micaceous quartzite, graphite mica schist, biotite schist and
muscovite schist. The upper Unit III is mainly composed of chlorite schist.
Based on the field observation, lithologic trends and mineral variation, the
stratigraphic succession of the investigated area can be described in Table (1) and the
distribution of rock units is shown in Fig. (3).
Table (1). Stratigraphic succession of the study area
Stratigraphic Units Age
Sedimentary Unit
Alluvium
-unconformity
Recent
Ultramafic Rocks
Serpentinite
Metamorphic Unit
Unit III
Chlorite schist
Unit II
Sericite schist
Micaceous quartzite
Graphite mica schist
Biotite schist
Muscovite schist
Unit I
Garnet biotite schist
Garnet muscovite schist
Garnet quartzite
Late Cretaceous-Early Eocene
Katha
Metamorphics
Late Jurassic-Early Cretaceous
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November 29-30, 2018, Hinthada University, Hinthada, Myanmar
EXPLANATION
Sedimentary Unit
Unconformity
Metamorphic Unit
(Katha Metamorphics)
Vertical Scale 0.8 ʺ = 1000 m
Horizontal Scale 1ʺ = 1250 m
Unit I Garnet biotite schist, garnet muscovite
schist and garnet quartzite
Unit II Quartz sericite schist, micaceous
quartzite, graphite mica schist,
biotite schist and muscovite schist
Unit III Chlorite schist
Alluvium Recent
Late Jurassic-
Early
Cretaceous
Village
1 km
Figure (3). Map showing the distribution of various rock units in the Ka Ka-Naung Pein –
Man Hlwe area
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Petrogenesis of Metamorphic Rocks
Types of Metamorphism
The type of metamorphism of study area is regional metamorphism and locally
dynamic metamorphism according to the mineralogical and textural criteria. The regional
metamorphic rocks of the present area consisting of platy or prismatic minerals, like micas
and chlorite, therefore exhibit strong schistosity.
In the study area, the characteristics features of regional metamorphism and dynamic
metamorphism in the field and petrographic studies are as follows:
(1) Texturally, the rocks of the study area show foliation and it is one of the most prominent
features of regional metamorphism;
(2) Successive mineral zones are formed, and appearance and disappearance of minerals from
zone to zone are taken into account the regional metamorphism;
(3) The deformation features of grain granulation, suture boundary, undulatory extinction and
intensely fractured grains are present locally and it provide the evidences of dynamic
metamorphism.
Mineral Assemblages, Metamorphic Facies and Zone
Six representative mineral assemblages are recognized in the study area based on the
petrographic analysis. They are as follows;
(1) chlorite -muscovite -quartz,
(2) biotite-muscovite- quartz,
(3) biotite-muscovite-chlorite-quartz,
(4) garnet-biotite-muscovite-quartz-graphite,
(5) garnet- muscovite -quartz,
(6) garnet- biotite-quartz,
The facies classification, nomenclature and representative mineral assemblages used
in this research work was mainly based on Turner (1968), Yardley (1989), Bucher and Frey
(1994), Winter (2010) and Bucher and Grapes (2011).
The mineral assemblage of Chl-Ms-Qtz is typical assemblage of chlorite schist. The
occurrence of this mineral assemblage in chlorite schist clearly indicates that the rock
develops in chlorite zone of lower greenschist facies.
The Bt-Ms-Qtz assemblage is developed in the biotite schist and Bt-Ms-Chl-Qtz in
muscovite schist. These assemblages are the characteristic of biotite zone of upper
greenschist facies.
Grt-Bt-Qtz assemblage is common in garnet biotite schist, Grt-Ms-Qtz assemblage in
garnet muscovite schist and Grt-Bt-Ms-Qtz assemblage in garnet quartzite. These
assemblages are typically developed in the metapelite of garnet zone of lower amphibolites
facies.
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Table (2). Mineral assemblages and metamorphic facies of the study area
Type of
Metamorphism
Rock Group Representative
Rock
Mineral
Assemblage
Metamorphic
Facies
Regional
Metamorphism
Metapelites
Chlorite schist
chlorite,
muscovite,
quartz Greenschist
Facies Biotite schist
biotite, muscovite,
quartz
Muscovite schist biotite, muscovite,
chlorite, quartz
Garnet biotite
schis
garnet, biotite,
quartz
Amphibolite
Facies
Garnet
muscovite schist
garnet,
muscovite,quartz
Garnet quartzite garnet,biotite,
muscovite, quartz
Reaction-Isograds
Chlorite zone
Pelites in the chlorite zone are typically slates and they contain chlorite and muscovite
with variable amounts of quartz and albite. In the study area, metapelites of the chlorite zone
are mainly composed of chlorite, muscovite and quartz. This assemblage is plotted on the
AKF diagram shown in (Fig. 4) (in Winter, 2010). Most of the analyzed pelite compositions
contain quartz, chlorite and phengitic muscovite in the two-phase field in (Fig. 4). In this
figure, Chl-Ms tie-lines connect coexisting chlorite and mica compositions. These
compositions are governed by the substitution of Al with Fe, Mg and Si, as a function of the
Al-content of the rock. Equilibrium is difficult to attain in experiments at these low
temperatures, so that P-T conditions are not certain, but they are believed to be in the 350 to
450°C range (Winter, 2010). The development of mineral assemblage and above
considerations, the chlorite zone is placed below the biotite isograd in P-T space.
Figure (4). AKF diagram showing mineral assemblage developed in chlorite schist (source:
Winter, 2010)
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Biotite zone
Many reactions can produce biotite. One biotite isograd reaction that can affect pelites
is encountered at point 2 in (Fig.7). The first prograde biotite taking places in common pelite
can be described by the reaction;
3Chl + 8Kfs = 5Bt + 3Ms + 9Qtz + 4H2O
Because chlorite is more plentiful than K-feldspar in most pelites, the above reaction
typically marks the loss of Kfs toward higher grade. This reaction can be demonstrated
geometrically by resorting to the AKF projection (Fig.5). At grades below this biotite-isograd
reaction, Chl and Kfs are stable together, as indicated in (Fig.5 a) by the tie-lines connecting
them. Above the isograd (Fig. 5 b), the new Bt-Ms tie line separates Chl and Kfs, so that Bt
+ Ms are stable together and Chl + Kfs are not, as this reaction indicates (in Winter, 2010).
According to Winter (2010), the metamorphic grades above the tie line flip reaction in
(Fig. 5), the composition of the white mica that coexists with biotite and chlorite gradually
becomes less phengitic via continuous reactions by which the most Al-poor white mica
breaks down, and the amount of chlorite and biotite increases. Biotite begins to appear in
progressively more aluminous pelites compositions as a result of the continuous reaction such
as the above reaction.
Near 400°C, the first biotite appears in Al-poor metapelites. Biotite forms at the
expense of Kfs and Chl. The reaction has equilibrium conditions of 420°C at about 0.35 GPa
in pure KFASH system. The equilibrium conditions of this reaction in the pure KFMASH
system are shown in (Fig.6) (Bucher and Grapes, 2011).
Figure (5). AKF diagrams illustrating the mineral assemblages developed in biotite zone
(source: Winter, 2010)
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Figure (6). P-T-X diagram representing the Kfs-Ms-Bt-Chl assemblage (Source: Bucher and
Grapes, 2011)
Figure (7). Petrogenetic grids showing the location of selected reaction isograds appropriate
for the study area. (Source: Winter, 2010)
Garnet zone
Garnet may become stable in the Mg-free KFASH system due to any of several
reactions. Garnet-isograd reaction giving way to produce assemblage, if Fe-chlorite is less
aluminous it may break down to almadine plus a small amount of Fe-biotite;
3Chl + 1Ms + 3Qtz = 4Grt + 1Bt + 12H2O
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This reaction has been suggested by Thompson and Norton (1968) and they described
this reaction is common in more typical pelites (in Winkler, 1979). This assemblage is
illustrated by means of AFM diagram as shown in (Fig.8).
Figure (8). AFM diagram showing the mineral assemblage occurred in garnet zone (Source:
Winter, 2010)
The first garnet appears in metapelites at temperature of around 450°C. This
temperature is in conflict with the formation provided by the pure FASH system. But, a
significant spessartine and grossular components in almadine garnet has the effect of
lowering temperature of first formation. Therefore, the Mn-Fe garnet appears at significantly
lower temperatures than pure almadine garnet. The porphyroblasts of almadine garnets do not
occur until the temperature of 460-500°C in typical pelites.
Fe-rich chlorite begins to be replaced by garnet + biotite between 500°C and 520°C.
The new assemblage Grt + Bt remains stable to very high grade and the P-T condition of this
garnet isograd reaction can be observed in (Fig.8). So, this reaction takes place at about
520°C and the metamorphic grade starts to enter the lower amphibolites facies.
Original Rock Sequence and Age
In general, various mineral assemblages, lithologic characters and some textural
features suggest that the metamorphic rocks in the study area may probably be
metamorphosed from mixture of pelitic and psammitic rocks. Following points are taking
into account the above conclusion.
(1). Characteristic minerals of greenschist facies include the chlorite, muscovite, biotite,
garnet and quartz. Greenschist derived from pelites have much more quartz and white
muscovite, less chlorite.
(2). Garnet bearing quartzite derived from the quartzose sandstone or quartzite.
(3). Graphite schist may come from organic rich sediment. The presence of graphite is
generated during the metamorphism of black shale and marls.
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(4). The abundant constituents of garnet in schists indicate rich in Fe and Mn component in
parent rock.
(5). Sequential interlayered nature of schist and quartzite indicates that the original rock
sequence may probably be alternative sequence of pelitic and quartzose sandstone.
(6). Continuous changing of mineral zoning in present area suggests that sediments are
homogeneous in composition and clay rich pelite.
These facts collectively suggest that the metamorphic rocks in study area may
probably be derived from pelite and psammite.
There are no radiometric ages available for any of the rocks described in present area,
so that original age of rock is not fixed. Form the various point of views, correlation with
other established area and similarity of metamorphic rock units exposed in the surrounding
area, the age of the metasediments in present area is equivalent to the Ngapyawdaw Chaung
Formation of Late Jurassic to Early Cretaceous.
Time of Metamorphism
There is not available precise time of metamorphism for the metamorphic rocks of
study area. Radiometric dating was carried out the metamorphic rocks exposed in some parts
of Katha and Kumon Range by GIAC project. Therefore, the time of metamorphism of the
present area can be ascertained to correlate with the neighboring area and some established
area concerning with this.
(1). The Jade Mine area, northwestern part of the study area, glaucophane bearing schist
associated with ultrabasic rocks is overlain by the Tertiary clastic sediments (Chhibber,
1934; Soe Win, 1960 in Aung Win, 2008).
(2). Mitchell (1998) established that the metamorphic rocks in Katha-Gangaw Range may be
Pre-Triassic rocks equivalent to the lower part of the Mergui Nappe or Chaungmagyi
Turbidities to the east.
(3). The metamorphosed rocks associated with ophiolite suite including radiolarian chert in
Tagaung- Myitkyina belt is derived from Ngapyawdaw Chaung Formation assigned the
age of Late Jurassic to Early Cretaceous from the analysis of radiolarian (Aung Kyaw
Thin, 2007) so that the age of the metamorphism of the area is later than assigned age.
(4). Radiometric dating were performed on metamorphic rocks, using Ar39
/Ar40
methods for
muscovite and biotite, in Katha and Kumon Ranges that indicate the time of
metamorphism took place in 37 to 32 Ma (G.I.A.C, 1999 in Aung Win, 2008).
(5). The earliest Alpine regional metamorphism in Himalaya Mountain chain is Late
Cretaceous in age (90-65 Ma). This event was responsible for the formation of eclogite
and blueschist in both continental and oceanic basement and Mesozoic sediments. The
peak of the Alpine metamorphism is usually interpreted as having ended in the early
Oligocene; younger, many Miocene ages have been obtained (Yardley, 1989 ).
Based on the above mentioned criteria, the time of metamorphism of the study area
could be assigned tentatively to Cretaceous to Early Eocene.
124 The Second Myanmar National Conference on Earth Sciences (MNCES, 2018)
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Table(3). Comparison of petrogenetic criteria and age of metamorphism of the rocks occurred
in the study area with those of other areas.
Previous Authors
Rock Type
(of which
geothermobarometric
calculation is
performed)
Peak
Metamorphic
Condition
Age of
Metamorphism
Aung Kyaw Thin
(2006)
Tagaung-Twinnge
Area
Basic Rock 1.1 GPa/ 650°C Late Cretaceous
Searl et al., (2007),
Mogok Metamorphic
Belt, Kyanigan and
Kyaukse Area
Gneisses 0.49 GPa/680°C
Late Jurassic-Early
Cretaceous/
Paleocene-Early
Eocene/
Late Eocene-Oligocene
Aung Win (2008)
Mogaung Area Basic Schist 2.3 GPa/493°C
Cretaceous-Early
Eocene
Nyan Win (2008)
Hopin-Mohnyin
Area
Pelitic Schist 1.9 GPa/750°C Late Eocene-Early
Oligocene
Chatterjee & Ghose
(2010)
Naga Hill
Basic Schist, Pelitic
Schist 2 GPa/610°C Eaerly Eocene
Thaire Phyu Win,
Indaw-Katha Area, Basic Schist 1.59GPa/583°C
Late Eocene-Early
Oligocene
Aung Khin Soe
(2018) KaKa-Naung
Pein-Man Hlwe area,
Katha Township
Pelitic Schist 0.35GPa/520°C Cretaceous to Early
Eocene
Conclusion
The occurrence of Chl-Ms-Qtz mineral assemblage in chlorite schist clearly indicates
that the rock develops in low-grade metamorphism of lower greenschist facies condition.
From biotite schist, through muscovite schist, garnet biotite schist, garnet muscovite schist
and garnet quartzite, the metamorphic grade gradually increased through lower greenschist
facies to lower amphibolites facies conditions. Although equilibrium is difficult to attain and
P-T conditions are not certain, the chlorite zone is to be in the 350 to 450°C range. The
equilibrium conditions of biotite zone are 420°C at about 0.35 GPa. The porphyroblasts of
almadine garnets do not occur until the temperature of 460-500°C in typical pelites and the
metamorphic grade starts to enter the lower amphibolites facies. The type of metamorphism
of study area is regional metamorphism and locally dynamic metamorphism according to the
mineralogical and textural criteria. The metamorphic rocks of the study area may probably be
metamorphosed from mixture of pelitic and psammitic rocks of the Ngapyawdaw Chaung
Formation of Late Jurassic to Early Cretaceous and the time of metamorphism could be
assigned tentatively to Cretaceous to Early Eocene. According to comparison of petrogenetic
criteria, the metamorphic grade of the Katha-Gangaw Range decreases toward the east.
The Second Myanmar National Conference on Earth Sciences (MNCES, 2018) 125
November 29-30, 2018, Hinthada University, Hinthada, Myanmar
Acknowledgements
I would like to express my thanks to Dr Thura Oo, Rector of Monywa University, Dr Sein Sein Aung
and Dr Thet Naing Oo, Pro-rectors of Monywa University and Dr Zaw Myint Ni, Professor and Head of
Geology Department, Monywa University for their encouragement. Thanks are also due to all local people of
the Ka Ka, Naung Pein and Manhlwe villages for their valuable helps through the field trip. Finally, all teaching
staff members from Geology Department, Monywa University are highly thanked for their cooperation.
References
Aung Kyaw Thin, (2006). Petrogenetic study on igneous and metamorphic rocks of the Tagaung-Twinnge area,
Thabeikyin Township. PhD, (Dissertation), Geology Department, Mandalay University,
Unpublished Paper, 123 p.
Aung Win, (2008). Petrogenetic studies of metamorphic rocks in Mogaung area, Mogaung and Phakant
Township, Myitkyina District, Kachin State. PhD, (Dissertation), Geology Department,
Mandalay University, Unpublished Paper. 183p.
Barker, A.J., (1998). Introduction to Metamorphic Textures and Microstructures.2nd ed. Staley Thorners
(Publishers) Ltd. UK.
Best, M.G., (2003). Igneous and Metamorphic Petrology. CBS publisher and Distributors, New Delhi, India.
Bucher, K. and Frey, M., (1994). Petrogenesis of Metamorphic rocks. 6thed, Springer-Verlag Berlin Heidelberg, printed in Germany.
Bucher, K. and Grapes, R., (2011). Petrogenesisof Metamorphic rocks.8thed, Springer-Verlag Berlin Heidelberg,
printed in Germany.
Hyndman, D.W., (1985). Petrology of Igneous and Metamorphic rocks.2nded. Mc.Graw Hill, Inc, New York.
Kerr, R.E., (1959). Optical Mineralogy. Mc. Graw Hill, Inc, New York.
Philpotts, A.R., (2003). Petrography of Igneous and Metamorphic Rocks. Waveland Press, Inc, UAS.
Turner, F.J., (1968). Metamorphic Petrology (Field and Mineralogical Aspects). Mc. Graw Hill, Inc, New York.
William, H., Turner, F.J., and Gilbert, C., (1953). Petrography. Freeman and Co., Sanfransisco.
Winter, J.D., (2010). An Introduction to Igneous and Metamorphic Petrology.2nd ed. Prentice Hall, New Jersey.
Yardley, B.W. D., (1989). An Introduction to Metamorphic Petrology. Longman Group Ltd.
Yardley, B. W. D., McKenzie, W. S., and Guilford, C., (1990). Atlas of Metamorphic Rocks and their Textures.Longman Scientific and Technical, John Wiley and Sons, Inc. New York.