The Igneous Rocks of the Mogok Stone Tract
A Ph.D. Dissertation by Kyaw Thu
Department of Geology, University of Yangon, Myanmar
Copyright © Kyaw Thu, 2007
Introduction from Bill Larson, Pala International
Kyaw Thu is a FGA gemologist with a Ph.D. in Geology. Pala International knows him from trips in the mid-1990s as one of the most interesting young gem enthusiasts, among so many wonderful students and collectors we met. Both Will and Bill Larson consider him a special and close friend. He has helped answer many questions regarding locality information for Brendan Laurs of GIA as well as meeting in person Dr. George Harlow of the American Museum of Natural History and corresponding with him for almost a decade. He has opened a gem laboratory and has applied to GIA to further his education. I was given a copy of his PhD thesis last month and Dr. Harlow made it available by scan for interested parties. Pala International is honored to share this with our readers.
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The Mogok Stone Tract is very famous not only for the finest rubies and spinels but also for gem quality sapphire, peridot, etc. The study area lies in the northeastern part of Mogok Stone Tract covering the Mogok–Kyat-pyin, Bernard–Pyaung-gaung and On-dan areas. It is a mountainous region with two distinct valleys—Mogok Valley and Kyat-pyin Valley. Both valleys were formed by structural and lithologic controls; they are south-plunging synclinal valleys separated by an anticlinal ridge (Baw-padan Anticline). These two valleys contain a larger proportion of placer gemstones.
The geology and the rock sequence of the area, modified from some previous works, and three new geological maps are presented. The rock sequence of the major rock units established is (from older to younger): Mogok metamorphics (metamorphosed Lower Paleozoic rock units—metamorphic age Late Oligocene), ultramafic and mafic rocks (Jurassic?), leucogranite (Early Oligocene), syenitic rocks (Late Oligocene), Kabaing Granite (Middle Miocene), and pegmatites and aplites (Middle Miocene).
On the basis of detailed microscopic observations, modal analyses, and normative calculations, the various igneous rock types according to IUGS and Williams et al. classifications are dunite, harzburgite, pyroxene peridotite, and hornblende peridotite for ultramafic rocks; quartz syenite, alkali-felspar syenite, nepheline syenite, alkali-felspar syenite pegmatite, and quartz monzonite for syenitic rocks; urtite, ijolite, and jacupirangite for urtite series; augite-biotite granite, leucogranite and biotite microgranite (Kabaing Granite) for granitic rocks; pegmatites and aplites. The pegmatites are complex, belonging to rare-element class, beryl type.
|7.5 x 5.0 x 4.5 cm. From the collection of Bill Larson. (Photo: Mia Dixon)|
On the basis of petrogenetic interpretations the igneous rocks of the area are mainly calc-alkaline and only partly alkaline. This is also evident from the bimodal distributions of the petrochemical data plots. The value of alkali-lime index (Peacock index) is 55 for the igneous rocks of the area, indicating the calcic to alkalic-calcic character in this area. ACF diagram and some distinctive chemical properties of the granitic rocks of the area indicate that these granitic rocks are mostly S-type granites.
In K2O mol. vs Na2O mol. variation diagram, the plots of leucogranite, biotite microgranite and pegmatite fall in the field of late-kinematic granite. According to the petrochemical data, the granitic rocks of the area may be regarded as continental collision granites.
In the alkaline rocks of the area, the (Na2O+K2O)/Al2O3 ratio is less than 1; thus according to Hyndman classification (1985), these alkaline rocks fall in the miaskitic type, i.e., not peralkaline. The origin of nepheline syenite as small irregular bodies in the marginal zones of Mogok marbles near the contact with leucogranite (as in the Thurein Taung area) or with syenite (as in the area northwest of On-dan) can be explained by the well-known limestone syntexis model. In a similar way the rocks of the urtite series may have been formed by the assimilation and desilication of the leucogranite or syenite in contact with mafic-rich marbles.
The ultramafic rocks occur as layered intrusions in garnet-biotite gneiss in Bernard–Pyaung-gaung area. The ultramafic rocks of the area are considered to be not related to an ophiolite suite because of the absence of bedded chert, pillow lavas, basalt-diabase sheeted dyke swarms, and large-scale serpentinization.
Field and petrochemical data suggest that the leucogranite and syenitic bodies intruded forcefully along a highly deformed zone roughly extending NE-SW. The depth of emplacement is estimated to range from katazone to mesozone. Kabaing Granite which is a large microgranite body intruded later at a shallower depth.
Radiometric dates of zircon in four rock samples by U-Th-Pb method give 129± 8.2 Ma (Early Cretaceous) for augite-biotite granite, 32± 1 Ma (Early Oligocene) for leucogranite, 25 Ma (Late Oligocene) for foliated syenite, and 16± 0.5 Ma (Middle Miocene) for painite from the contact zone between leucogranite and marble.
It has been observed that the syenitic rocks and pegmatites are especially important for the formation of precious gemstones of the area. The important gemstones with regard to the various igneous rock types are aquamarine, topaz, danburite, amethyst, moonstone, zircon in pegmatites, sapphire in syenite pegmatites, peridot in peridotite, and painite in leucogranite (contact zone).
I acknowledge a special debt to Prof. Dr. U Thein (President, Myanmar Geoscience Society) for his guidance and suggestions for my research works.
I owe a debt of thanks to Dr. Aye Ko Aung (Professor/Head, Geology Department, Dagon University) for reading the manuscript and suggestions rendered. Thanks are also extended to U Htay Win (Associate Professor/Head, Department of Geology, Yangon University) for his care and valuable advice.
This dissertation came to fruition under the guidance of Professor Hla Kyi (Part-time Professor, Applied Geology Department) for reading the manuscript, his guidance, discussions and suggestions.
My special thanks are due to Professor Thein Win (Pro Rector, West Yangon University), Professor Maung Ko (Part-time Professor, Geology Department, Yangon University), and Dr. Khin Maung Myint (Professor/Head, Geology Department, Mandalay University) for reading of the manuscript, discussions and suggestions, for the improvement of this manuscript.
The author is grateful to Dr. Khin Zaw (Centre for Ore Deposit Research, University of Western Australia) for his generous help and suggestions for LA ICP-MS tests, X-RF and LRS tests during the research, and to Daw Ohh Mar Win (Lecturer, Universities’ Research Center) and to Dr. Moe Myintzu (X-RD section, D.A.E.) for the X-RF and X-RD results respectively.
Individuals who helped are also numerous; my heartfelt thanks are due to U Zaw Nyunt and U Thant Zin and U Nay Myo for providing facilities and warm hospitality during the field trips.
I wish to express my gratitude to Daw Thuzar Aung (Macle Gem Trade Lab.) for the help given throughout the study.
Last, but not least I would like to express my sincere thanks to my parents and all my teachers who guided me to reach such a position.
Chapter I Introduction
1.4 Method of Study
1.5 Previous Works
Chapter II Geology of the Area
2.2 Rock Sequence
Chapter III Petrography
3.4 Syenitic Rocks
3.5 Urtite Series
3.6 Kabaing Granite
Chapter IV Petrochemistry
4.1 Analytical Data
Chapter V Petrogenesis
Chapter VI Geochronology
Chapter VII Economic Geology
7.4 Peridot Deposits
Chapter VIII Summary and Conclusions
List of Figures in Chapters I and II (images from Pala International are not listed)
|1.1||Satellite image of the Mogok Stone Tract (scale: 1:500,000)|
|1.2||Three dimensional view of the geomorphology of the Mogok Stone Tract (TM image; 30 m resolution)|
|2.1||Regional geological map of the study area modified after Bender (1983)|
|2.2||Map showing MMB relative to blocks and plates in the Myanmar region (modified after Mitchell el aI., 2006)|
|2.3||Geological map of Mogok–Kyat-pyin area, geology by Kyaw Thu, 2006|
|2.4||Geological Map of Bernard–Pyaung-gaung area, modified after Thet Tin Nyunt (2000), Kyaw Thu (2006)|
|2.5||Geological Map of On-Dan area, modified after Thuzar Aung (2003), Kyaw Thu (2006)|
|2.6||(a) Highly weathered pegmatite exposure, Sakhan-gyi, 22° 54' 1.2" N, 96° 20' 56.1" E|
|(b) Dyke of pegmatite at Pan-taw; 22° 57' 47.3" N, 96° 24' 15.6" E|
|(c) Panoramic view of Kabaing Taung, inset; large block of biotite microgranite showing exfoliated nature at the peak, near Kabaing village|
|(d) Small outcrop of Kabaing Granite showing onion skin weathering, 22° 57' 14.9" N, 96° 24' 54.6" E, Kyauk-sin–Pan-taw area|
|(e) An outcrop of showing exfoliation nature in biotite microgranite, near On-dan village, 22° 57' 12.2" N, 96° 14' 38.05" E|
|2.7||(a) Phlogopite-diopside marble and urtite rocks contact in Thurein Taung, 22° 54' 12.2" N, 96° 22' 18.8" E; urtite exposure showing highly brecciated nature due to fault contact nature (inset)|
|(b) Urtite and white marble contact in Yadana-kadae-kadar mine, 22° 54' 34" N, 96° 22' 31" E ; mafic minerals mainly hornblende and nepheline in surface of urtite exposure (inset)|
|(c) Urtite intruded into the marble showing scapolite-diopside-graphite contact zone, 22° 54' 11.3" N, 96° 22' 17.3" E|
|(d) Pegmatite vein intruded into the urtite body, Thurein Taung, 22° 54' 12.4" N, 96° 22' 20.6" E|
|(e) Xenolith of nepheline syenite in urtite, Thurein Taung, 22° 54' 12.7" N, 96° 22' 20.7" E|
|2.8||(a) A distinct syenitic rocks exposure showing exfoliated nature in syenite exposure, north of Ohn-gaing village, 22° 56' 27.2" N, 96° 29' 36.8" E|
|(b) Syenite exposure at Kyauk-wa, north of Mogok|
|(c) Dyke of urtite in syenite exposure, north of On-dan, 22° 57' 16.4" N, 96° 14' 39" E|
|2.9||(a) A distinct exposure of leucogranite in Hin-thar Taung|
|(b) Photograph showing leucogranite and diopside-phlogopite marble contact to form the painite deposit in Wet-loo mine, 22° 54' 28.5" N, 96° 23' 34.9" E|
|(c) Highly weathered leucogranite exposed in Baw-mar mine|
|(d) An outcrop showing exfoliated nature in leucogranite, north of Baw-mar|
|(e) Photograph showing leucogranite intruded into the garnet biotite gneiss in Pan-taw, 22° 57' 44.6" N, 96° 24' 41.7" E|
|(f) Syenite vein in leucogranite about three feet in thickness, Wet-loo mine, 22° 54' 28" N, 96° 23' 35" E|
|2.10||(a) Panoramic view of the peridotite-dunite bodies, north-east of Bernard-myo|
|(b) Peridotite exposure showing false bedded nature, Mya-sein Taung, 23" 00' 03.4" N, 96" 27' 54.4" E|
|(c) Photograph showing peridotite partly altered to serpentinite due to the auto metamorphism, 22" 59' 55" N, 96" 27' 48.8" E|
|(d) An outcrop showing jointed nature in dunite, Pyaung-gaung, 23° 00' 40.5" N, 96° 28' 40.0" E|
|(d) Pegmatite dyke in peridotite and chrysoprase veins in upper part of photo, Mya-sein Taung, 23° 00' 10.5" N, 96° 27' 44.9" E|
|2.11||(a) Panoramic scenery of Taung-me Taung; augite biotite granite exposure at the peak of Taung-me Taung (inset), 22° 58' 18.4" N, 96° 28' 8.5" E|
|(b) Augite-biotite granite exposure showing the distinct faulted nature in Shwe-u-daung taung; inset: small quartzo feldspathic vein cross cut in foliated augite-biotite granite, north of On-dan village, 23° 01' 12.1" N, 96° 13' 19.07" E|
|2.12||(a) Photograph showing mullion structure in calc-silicate rock due to the thrusting, east of Gwe-bin, 22° 53' 44" N, 96° 22' 24" E|
|(b) Dyke of urtite showing folded nature in marble indicates that effected by tectonism, Kyauk-saung, 22° 55' 21" N, 96° 25' 53" E|
|(c) The exposure showing Mogok thrust, north-west directed thrust plane at north of Mogok, 22° 56' 37.5" N, 96° 31' 22" E|
|(d) Close-up view of photo|
|(e) Showing footwall carbonate mylonite along the thrust zone|
|(f) Well jointed nature in phlogopite marble at Gwe-bin|
|Additional figures to be added with next installment|
List of Figures in Chapter III – Part 1 (images from Pala International are not listed)
|3.1||Small exposure of gabbro rock in Htan-saing, north of Bernard-myo, 22° 00' 25.6" N, 96° 25' 54.7" E|
|3.2||Mineral composition of the gabbro rock, XN, 10 X|
|3.3||Chrysoprase vein in dunite exposure, Mya-sein Taung UMEHL mine|
|3.4||Olivine (Ol) altered to serpentine (Sp) in dunite, XN, 25 X|
|3.5||(a) Photomicrograph showing mesh-like serpentine in olivine of dunite, XN, 10 X|
|(b) Close-up view of serpentine in photo (a), XN, 25 X|
|3.6||Photograph showing magnetite veins in peridotite outcrop at Pyaung-gaung, 22° 58' 16" N, 96° 33' 11" E|
|3.7||Olivine with chrysotile veinlets across the olivine in peridotite, XN, 10 X|
|3.8||Orthopyroxene (Opx) in peridotite, XN, 10 X|
|3.9||Olivine with chrysotile veins, orthopyroxene (Opx), clinopyroxene (Cpx) and anhedral chromite grain (Cm) in peridotite, XN, 25 X|
|3.10||Olivine with chrysotile veinlets across the olivine and amphibole (Amp) crystal in peridotite, XN, 25 X|
|3.11||Flaky serpentine (antigorite) in peridotite, XN, 25 X|
|3.12||Chrysotile occurs as cross fiber veinlets in peridotite, XN, 25 X|
|3.13||Mica flake in olivine grain, in peridotite, XN, 25 X|
|3.14||Antigorite crystals in chrysoprase (Chry) vein with magnetite, XN, 25 X|
|3.15||Radial chalcedony and magnetite grain in chrysoprase, XN, 25 X|
|3.16||Mesh-like serpentine and relic of olivine grains in serpentinized dunite, XN, 25 X|
|3.17||Mesh-like structure of serpentine minerals in serpentinite at Mya-sein-Taung, XN, 25 X|
|3.18||Photograph showing highly jointed nature in augite-biotite granite at the peak of Taung-me Taung 22° 58' 18.4" N, 96° 28' 8.5" E|
|3.19||Twinned plagioclase (Pgl), augite (Aug) and quartz grains in augite-biotite granite, Taung-me Taung; between XN, 10 X|
|3.20||Subhedral zoisite (Zoi) crystal in augite (Aug)-biotite granite, Shwe-u-daung Taung; (a) P.P.L. (b) XN, 25 X|
|3.21||Anhedral garnet (Gar) grain and biotite (Bio) flakes in augite-biotite granite, Pan-yaung, P.P.L., 10 X|
|3.22||Sericitization occurs along the cleavage planes and fan shape sericite (Seri) in border of k-feldspar, XN, 25 X|
|3.23||Photograph showing hillock nature of marble unit in leucogranite body, NE of Dattaw Taung, 22° 57' 56.2" N, 96° 32' 29" E|
|3.24||Painite crystal in k-feldspar, near the contact of leucogranite and marble, Wet-loo, PPL, 25 X|
|3.25||K-feldspar with string perthitic texture (pe) in leucogranite, XN, 10 X|
|3.26||Interstitial calcite (Cc) grains among k-feldspar (Or) and quartz (Q) with augite (Aug), near contact of marble unit, XN, 10 X|
|3.27||K-feldspar with string perthite (pe) with myrmekitic (m-q) intergrowth of plagioclase feldspar and quartz, Htin-shu Taung, XN, 25 X|
|3.28||Anhedral garnet (Gar) grain with quartz (Q) inclusions in leucogranite, Hin-thar Taung, P.P.L., 10 X|
List of Figures in Chapter III – Part 2 (images from Pala International are not listed)
|3.29||Anhedral aegirine augite (Aug) grain in quartz syenite, PPL, 10 X|
|3.30||Quartz syenite containing alkali feldspar (Or), aegirine augite (Aug), and quartz (Q), XN, 10 X|
|3.31||Anhedral garnet (Gar) grain, iron ore and biotite (Bio) showing foliation in quartz syenite, PPL, 10 X|
|3.32||Anhedral and basal section of scapolite grains in quartz syenite from contact zone, XN, 10 X|
|3.33||Myrmekitic intergrowth of quartz and plagioclase feldspar in quartz syenite, XN, 25 X|
|3.34||Myrmekitic (m-q) intergrowth of quartz and feldspar, and biotite (Bio) in alkali-feldspar syenite, XN, 25 X|
|3.35||K-feldspar showing grid twinning with patch perthite (pe) in alkali-feldspar syenite XN, 25 X|
|3.36||Subhedral nepheline (ne) crystal in foid-bearing alkali-feldspar syenite, XN, 10 X|
|3.37||K-feldspar with perthitic (pe) veinlets and opaque mineral in quartz syenite, XN, 25 X|
|3.38||Euhedral sphene crystals in alkali-feldspar of foid-bearing alkali-feldspar syenite, PPL, 25 X|
|3.39||Euhedral plagioclase (Pgl) crystal showing polysynthetic twinning in alkali syenite pegmatite, On-dan, XN, 25 X|
|3.40||K-feldspar with flame perthite (pe) enclosing zircon crystal and corundum grain, On-dan, XN, 25 X|
|3.41||K-feldspar (Or) with flake perthite (fl-pe) in alkali-syenite pegmatite, XN, 25 X|
|3.42||Garnet (Gar) and biotite (Bio) flakes in alkali-syenite pegmatite, Lay-thar, PPL, 10 X|
|3.43||Corundum (C) crystal enclosed in spinel (Sp), alkali-syenite pegmatite, Lay-thar, PPL, 10 X|
|3.44||Corundum showing typical three sets of short rutile (Ru) needles and small zircon (Zr) inclusions in alkali-syenite pegmatite, PPL, 25 X|
|3.45||Plagioclase (Pgl) showing pericline twinning in quartz monzonite, XN, 10 X|
|3.46||Complex polysynthetic twinning in plagioclase (Pgl) and augite in quartz monzonite, XN, 10 X|
|3.47||Hornblende and pyroxene and the rest white colour is nepheline in urtite, PPL, 25 X|
|3.48||Pyroxene is partly altered to hornblende in urtite rock, PPL, 25 X|
|3.49||Calcite showing twinning and amphibole in urtite, XN, 25 X|
|3.50||Euhedral biotite crystal in urtite, XN, 25 X|
|3.51||Amphibole showing simple twin in urtite, XN, 10 X|
|3.52||Rectangular shaped nepheline, hornblende and calcite in urtite, XN, 10 X|
|3.53||Anhedral deep yellowish brown, titanium rich melanite garnet and augite in urtite, PPL, 10 X|
|3.54||Mineral constituents of the ijolite containing hornblende, augite, nepheline, iron ore and plagioclase feldspar, XN, 10 X|
|3.55||Feldspar showing combination of Carlsbad and albite twin, hornblende and nepheline in ijolite, XN, 10 X|
|3.56||Euhedral zircon crystal in nepheline, PPL, 25 X|
|3.57||Small corundum grains in ijolite, Thurein Taung, PPL, 25 X|
|3.58||Mineral constituents of jacupriangite include hornblende, pyroxene, and plagioclase showing pericline twinning, XN, 10 X|
|3.59||Basal section of hornblende in jacupriangite, XN, 25 X|
|3.60||Kabaing granite intruded into the dunite body in Pyaung-gaung, 23° 00' 18.4" N, 96° 27' 8.5" E|
|3.61||Mineral constituents of biotite microgranite includes quartz, feldspar and biotite mica, XN, 10 X|
|3.62||Euhedral alkali-feldspar shows zoning with some biotite in Kabaing granite, XN, 10 X|
|3.63||Chlorite, alteration product of biotite in Kabaing Granite, PPL, 25 X|
|3.64||Elongated bioite crystal showing bent nature due to deformation, 52 XN, 25X|
|3.65||Granophyric quartz (Q) in K-feldspar, XN, 10 X|
|3.66||Graphic quartz (Q) in k-feldspar and the quartz protrudes in the orthoclase (Or) by forming indentations, XN, 10 X|
|3.67||Graphic quartz (Q) with extinctions into the k-feldspar, XN, 10 X|
|3.68||K-feldspar with perthite. Both the high proportion of perthite to k-feldspar and the irregular shapes rather suggest a metasomatic origin for the plagioclase. K-feldspar in the extinction position, XN, 10 X|
|3.69||K-feldspar showing rare sector twin and intergrowth with quartz, XN, 25X|
|3.70||Chalcedonic silica vein in k-feldspar in aplite, XN, 25 X|
|3.71||Plotted data of the igneous rocks in the Mogok Stone Tract, except ultramafic rocks (source; IUGS Classification, 2006)|
|3.72||Modal classification of ultramafic rocks based on the proportions of olivine (Ol), orthopyroxene (Opx), clinopyroxene (Cpx), pyroxene (Px) and hornblende (Hbl) (source: IUGS Classification, 2006)|
List of Figures in Chapter IV (images from Pala International are not listed)
|4.1||Sample location map of the Mogok Stone Tract (source; Landsat TM image, 30m resolution, band combination 754)|
|4.2||Variation diagram of major elements vs SiO2 in igneous rocks of the study area (cont.)|
|4.3||Na2O/K2O vs SiO2 variation diagram, showing the trend of differentiation (KT-1 to KT-9 are granitic rocks/KT-10 to KT-15 are syenitic rocks and KT-16 to KT-23 are mafic to ultramafic rocks)|
|4.4||Percent anorthite in normative plagioclase plotted against the Thornton-Tuttle differentiation index (KT-1 to KT-9 are granitic rocks/KT-10 to KT-15 are syenitic rocks and KT-16 to KT-23 are mafic to ultramafic rocks)|
|4.5||Alkali-lime index diagram for granitic, syenitic, basic and ultramafic rocks (Peacock index)|
|4.6||Alkali-lime index diagram for granitic, basic and ultramafic rocks (Peacock index)|
|4.7||Major element discrimination of igneous rocks supposed to be collision-related, subdivided as alkaline, calc-alkaline and strongly peraluminous, and highly fractionated calc-alkaline (after Sylvester, 1989)|
|4.8||Al2O3 — CaO — (Na2O+K2O) diagram|
|4.9||Normative Ab-Or-An diagram for the igneous rocks of the study area, with dividing lines according to O’Connor (1965)|
|4.10||Plot of Wright’s (1969) alkalinity index Al2O3+CaO+Na2O+K2O/Al2O3+ CaO-Na2O+K2O solid line and field names are after Wright, and the dashed line, separates alkaline from calc-alkaline, after Khin Zaw (1986)|
|4.11||Diagram showing K2O vs SiO2 wt % ration for granitic rocks and syenitic rocks of the study area
Calc-alkaline – Jake and Gill (1970)
Alkaline (1) – Gried and Lefeure (1972)
Alkaline (2) – Lemoitre (1962)
|4.12||Fe(t)-Na2O+K2O—MgO (AFM) diagram, in terms of alkalis, total Fe and Mg for the igneous rocks of the study area|
|4.13||ACF diagram for the granitoids of the study area (after Hyndman, 1985); Molar ratio: A = Al2O3-Na2O-K2O, C = CaO, F = Fe2O3+MgO|
|4.15||General Ca – Na – K compositional difference between the main kinds of alkaline igneous rocks; rocks become more mafic rich towards the Ca corner of the diagram (after Hyndman, 1985)|
|4.16||SiO2-(Na2O+K2O) – (FeO(t)+MgO) diagram|
|4.18||Normative Qt-Ab-Or-H2O ratios of igneous rocks from the study area. Diagram showing H2O saturated liquidus field boundaries and isobaric temperature in the system Qtz-Ab-Or-H2O for various water pressures (after Tuttle and Bowen, 1958)|
|4.19||Temperature – differentiation index diagram for the igneous rocks of the study area, at 2 kb water pressure (after Piwinskii and Wyllie, 1970)|
|4.20||K2O mol. vs Na2O mol. variation diagram of granitic rocks in the area, showing the fields of syn-kinematic and late-kinematic granites (after Marmo, 1956)|
|4.21||Schematic depth-temperature relation diagram (after Marmo, 1969)|
List of Figures for Chapters V and VI (images from Pala International are not listed)
|5.1||K2O vs SiO2 diagram for granitoids of the study area; distinction between oceanic plagiogranite and other granitoids from the other environment (after Maniar and Piccoli, 1989)|
|5.2||Al2O3 vs SiO2 diagram for granitoids of the study area (after Maniar and Piccoli, 1989)|
|5.3||MgO vs SiO2 diagram for granitoids of the study area (after Maniar and Piccoli, 1989)|
|5.4||Shand’s index diagram for granitic rocks of the area. Distinction between CCG and CAG+IAG (after Maniar and Piccoli, 1989)|
|6.1||(a) LA ICP-MS, (b) BSE image of zircon crystals, (c) LA ICP-MS technique|
|6.2||(a, b, c) Data interpretation processes of zircon dating in LA ICP-MS and SHRIMP techniques|
|6.3||(a, b) Data interpretation processes of zircon dating in LA ICP-MS and SHRIMP techniques|
|6.4||The concordia plot diagram of radiometric dating of augite-biotite granite (A-2) by LAICP-MS technique|
|6.5||Location map and 40 Ar/39 Ar diagrams of dated samples form high grade metamorphic and intrusive rocks of Mogok area; all the ages from this area are Early to Middle Miocene (after Bertrand et al., 2001)|
List of Figures for Chapter VII (images from Pala International are not listed)
|7.1||Location map of the pegmatitic gem deposit mines and other mines of Mogok Stone Tract|
|7.2||Highly weathered phlegmatic dyke exposure in Sakhan-gyi, 22° 54' 1.2" N, 96° 20' 56.1" E|
|7.3||Entrance of adit in phlegmatic mine, Sakhan-gyi, 22° 54' 1.2" N, 96° 20' 56.1" E|
|7.4||Illegal mines (Lay-bin-dwin) in phlegmatic deposit, since 2004, Sakhan-gyi, 22° 54' 02.1" N, 96° 20' 51" E|
|7.5||Searching the gems from phlegmatic, Sakhan-gyi, 22° 54' 02.1" N, 96° 20' 51" E|
|7.6||Lay-bin-dwin in phlegmatic mine, Sakhan-gyi, 22° 54' 02.1" N, 96° 20' 51" E|
|7.7||Phlegmatic with topaz,quartz, clevelandite, cassiterite and feldspar, Sakhan-gyi|
|7.8||Phlegmatic dyke at pan-taw area, entrance of adit in phlegmatic body and drilling in Kabaing Granite for blasting processes (in-set), 22" 57' 47.3" N, 96" 24' 15.6" E|
|7.9||(a) Large aquamarine crystal (21 ern in length), Sakhan-gyi; (b) rough aquamarine 134 g; (c) after faceted, 119 carats from Pein-pyit|
|7.10||(a) Topaz crystal in phlegmatic groundmass; (b) some big terminated topaz crystals; (c) topaz crystal penetrates in quartz with muscovite at the base; (d) unusual aquamarine cat’s eye, 90.80 carats, from Sakhan-gyi; (e) herderite crystal, 23.02 carats; (f) rough (120 g) and faceted (6.202 carats) yellow scheelites; (g) large elongated quartz crystal (10 cm in length); (h) large goshenite crystal, 8 x 6 x 4 cm, shows prism, pyramid and basal pinacoid|
|7.11||(a) Aquamarine, quartz and cleavelandite in phlegmatic matrix from Pan-taw; (b) phlegmatic with hematite and topaz; (c) phlegmatic with, cassiterite, c1eavelandite, muscovite and quartz from Pan-taw; (d) faceted sherry coloured topaz; (e) amazonite crystals in phlegmatic groundmass from Pan-taw phlegmatic deposits|
|7.12||(a) Ilmenorutile crystal and its X-RD spectrum; (b) rhodochrosite crystals and its X-RD spectrum; (c) colour-change fluorite from Pan-taw phlegmatic deposit|
|7.13||The miners digging the sapphire from alkali yemenite phlegmatic dyke in Buga mine, On-dan, 22° 59' 7" N, 96° 12' 51" E|
|7.14||Close-up view of sapphire bearing alkali yemenite phlegmatic dyke intruded into the phlogopite marble at Buga mine, On-dan|
|7.15||Sapphire-bearing alkali yemenite phlegmatic (highly weathered) dyke intruded to the leucogranite in Buga|
|7.16||Sapphire crystal associated with schorl in feldspar groundmass in alkali yemenite phlegmatic|
|7.17||Sapphire crystal with “black silk” in feldspar ground mass of nepheline yemenite, On-dan|
|7.18||(a) Large sapphire crystal; (b) sapphire package from UMEHL mine, On-dan|
|7.19||Panoramic view of Thurein Taung|
|7.20||Geological sketch model of Thurein Taung|
|7.21||Sapphire is enclosed by purplish spinel (X-RD result) from alkali yemenite phlegmatic, Thurein Taung|
|7.22||(a,b,c) Sapphires in alkali-feldspar groundmass of alkali-feldspar yemenite phlegmatic, Thurein Taung|
|7.23||Alkali yemenite phlegmatic dykes intruded in calc-silicate rocks and local miners digging sapphires from highly weathered alkali yemenite phlegmatic, JV mine of Lay-thar, 23° 00' 26.3" N, 96° 30' 19.5" E|
|7.24||Sapphires embedded in alkali feldspar groundmass of alkali yemenite phlegmatic, Lay-thar JV mine|
|7.25||Local miners searching the sapphires in Lay-thar JV mine, 23° 00' 26.0" N, 96° 30' 19.0" E|
|7.26||Fluid and silicate-melt inclusions of sapphires form alkali yemenite phlegmatic deposits, Mogok. (25 X, transmitted light and dark field)|
|7.27||Plotting diagram of Cr2O3/Ga2C (%wt) vs Fe2O3/TiO2(%wt) ratios shows the different populations and overlapping features of basaltic and non-basaltic blue sapphires (source: GAAJ)|
|7.28||Photograph showing the peridot mine and miners digging the dunite in entrance of the adit at Mya-sein Taung, 23° 00' 03.4" N, 96° 27' 54.4" E|
|7.29||Entrance of the tunnel and railway (made in local miners) used for carrying of peridotite-dunite wastages, Mya-sein Taung, 23° 00' 07.5" N, 96° 27' 51.0" E|
|7.30||Photograph showing the pocket nature of peridot deposit in dunite, although no gems in pocket locally called “Owe-poke” and filled only talc|
|7.31||Peridot crystal in dunite groundmass of fragment of pocket deposit from Zalat Taung|
|7.32||Aragonite with peridot from pocket deposit of dunite and its X-RD spectrum, Mya-sein Taung|
|7.33||Magnesiohornblende crystals, associate minerals of peridot, and its X-RD spectrum, Mya-sein Taung|
|7.34||(a, b) Gem quality peridot crystals from pocket type deposits, UMEHL mine, Mya-sein Taung; (c) rough peridot, 68 carats; (d) after faceted peridot 43 carats|
|7.35||Gem quality peridot lot from pocket type deposit, UMEHL mine, Mya-sein Taung and display in UMEHL Emporium|
|7.36||Marble and leucogranite contact indicate painite deposit at Wet-loo mine, 22° 54' 28.5" N, 96° 23' 34.9" E|
|7.37||Dealer purchasing painite from local miners, near Wet-loo mine|
|7.38||Dealer checking the painite by eye-side from local miners, near Wet-loo mine|
|7.39||Painite and rubies in leucogranite matrix, near Wet-loo mine|
|7.40||Huge painite aggregate with rubies from Thurein Taung|
|7.41||(a) Gem quality painite crystals; (b) painite shows prism, pyramid and pinacoid faces; (c) faceted painite (3.5 cts.) from Thurein Taung; (d) faceted painite from Namya, 0.59 cts.; (e) pleochroism effect of painite from Thurein Taung|
|7.42||Anatase crystal, shows blue colour, associated with painite from Thurein Taung|
|7.43||Baddeleyite crystal, associated with painite and its XRD spectrum from Thurein Taung|
|7.44||(a) Two-phase inclusion, transmitted light, 30 X; (b) rectangular shape liquid filled negative inclusions, transmitted light, 30 X ; (c) needle-like rutile inclusions, transmitted light, 30 X; (d) baddeleyite crystal inclusion in painite, transmitted light, 30 X ; (e) BSE image of srilankite inclusion in painite from Namya; (f) srilankite crystal inclusion in painite from Wet-loo, transmitted light, 30 X|
List of Tables
|2.1||Major geological succession of the study area|
|3.1||Classification of pegmatites of the rare-element class for Sakhan-gyi and Pan-taw area, after Cerny (1991)|
|4.1||Chemical composition and norms of the igneous rocks from the Mogok are (in wt%)|
|6.1||LA ICP-MS: U-Pb zircon age data for leucogranite (LG-1) and zircon inclusion in painite, associate with ruby in leucogranite matrix (P-1)|
|6.2||Comparison of rock sequence in southern part of Mogok Stone Tract and the study area with radiometric ages|
|7.1||Genetic classification of gemstones from the Mogok Stone Tract|
|7.2||Various types of gemstones associated with igneous rocks|
|7.3||Classification of granitic pegmatites (modified after Cerny, 1991)|
|7.4||Classification of granitic pegmatites of the rare-element class (Cerny, 1991)|
|7.5||Classification of pegmatites of the rare-element class, beryl type for Sakhangyi and Pan-taw|
|7.6||Physical and optical properties of gemstones from Sakhan-gyi and Pan-taw pegmatites|
|7.7||Trace elements in sapphires from selected localities tested using LA- ICP-MS method|
|Gem quality in matrix, 9 x 7 cm. The crystal measures 3.4 cm! From the collection of Bill Larson. (Photo: Mia Dixon)|
Chapter I Introduction
Any list of the classic, historically most important gem deposits of the world must include the Mogok Stone Tract. It is very famous not only for the world’s finest rubies and spinels but also for gem quality sapphire, peridot, etc. for many centuries. Sapphires are most abundant in Pan-sho, Kyat-pyin, Kyauk-pyat-that, Baw-mar, Lay-thar, and Ondan areas, peridot is limited to the area of Bernard–Pyaung-gaung, 10 km north-northwest of the Mogok Valley. Gem quality apatite, scapolite, moonstone, zircon, garnet, iolite, amethyst, danburite, etc. and some rare gemstones, painite, poudretteite, etc. are also found in this area.
The Mogok Stone Tract lies in the northwest end of the Shan Plateau. The tract is sickle-shaped, with the vertical limb being formed by the Irrawaddy river. Its northern terminus is at the bend of the Shweli river, as it twists and bends, flowing at times from south to north into the Irrawaddy. The vertical limb of the tract extends south to north from Latitude 22° 54' 00" N up to 23° 01' 00" N, and the horizontal arm of the tract rubs along the Longitude 96° 12' 06" E as far as 96° 33' 30" E or approximately 380 km NNE of Naypyidaw, the capital of Myanmar, and also 200 km NE of Mandalay; refer to one-inch topographic maps no. 93 A/8, B/1, B/5, and B/9. The approximate length of the tract is about 37 km in E-W and width is about 13 km in N-S. Generally the study area can be divided into three different topographic units according to gemstone occurrences, viz: Mogok–Kyat-pyin area, Bernard–Pyaung-gaung area and On-dan area.
The general area of the tract is very mountainous, forming a sort of amphitheater. The high mountains to the north run almost east-west. Most of the mining takes place in the alluvia of floors and flanks of the Mogok and Kyat-pyin valleys. Mogok Valley is the most important, consisting of a narrow alluvial plain, 5 km long running northeast-southwest, and about 1 km wide.
|Three dimensional view of the geomorphology of the Mogok Stone Tract (TM image; 30 m resolution).|
Mogok–Kyat-pyin area is a mountainous region with two distinct valleys, Mogok Valley and Kyat-pyin Valley. The Mogok Valley is located at an elevation of 1158 m above sea level and the Kyat-pyin Valley is also located at 1350 m above sea level. East of the Kin chaung, the hills rise to massive ridges, which culminate in the Taungme Taung (2300 m), the highest point in the area; this peak dominates both the Bernard-myo (Ywa-thayar) and the Mogok Valley. It forms a pyramidal hill from which several ridges radiate in different directions. One of them, running east and south-east contains the Kyini Taung (2052 m) and Let-nyo Taung (1626 m), an arm of the above ridge, runs towards Mogok.
Dattaw Taung (1555 m) in the east of Mogok, Shwe-daing, Lin-yaung-chi to Kadoke-tat, Baw-padan, Kyauk-poke, Kyauk-saung, Pingu Taung (1186 m), Kyauk-pyatthat (1700 m) in the west of Mogok show typical fold pattern (anticline-syncline nature) and famous for primary ruby deposits. The hills north of Kyat-pyin form picturesque ridges cut by deep valleys, the western most ridge being the Baw-lone, Kyauk-pyat-that, Myaing-gyi Taung, running west-south-west towards Kabaing. In this area, Kyauk-sin Taung forms the highest point. The typical feature is formed by the arc like or sinuous parallel ridges, which start from the east, run in an east-west direction, turn south in the centre and again run westwards.
Bernard (Ywa-thaya)–Pyaung-gaung area forms the highest elevation of the Mogok Stone Tract, 1585 m above sea level. Most of the area is mountainous, rugged with steep slopes at the higher region, whereas moderate slopes to lowland with rounded hills at the lower part. The Injauk valley runs through this area, where diverging arms of the Taung-me Taung form high ridges and peaks at the Maw-giwa Taung (2043 m). However, some isolated hills and ranges, such as Mya-sein Taung, Zalat Taung, Htinshu Taung and Lay-thar Taung are also found as distinct landmark and famous gem deposits of this area.
On-dan area occurs in the rugged and hard accessible territories of the hill regions, which are covered with dense forest. The most distinctive mountains are Shweu-daung Taung (1900 m), the highest peak in this area and Hnamataw-lay range. The Shwe-u-daung Taung takes a bend to the south, dividing Momeik from Mogok. Due north is Hnamataw-Lay range (approximately 1524 m high); to the south is a smaller hill, just 975 m high. Directly to the west are lower mountains that stretch to the Irrawaddy river, falling off as they approach the river.
|Three dimensional view of the geomorphology of the Mogok Stone Tract (TM image; 30m resolution).|
In the study area drainage falls into two different systems. The first system starts from the northern watershed of the rugged, hilly and mountainous terrain and flowing from south to north, and then flowing into the Shweli river. Laung-zin chaung, On-dan chaung, Kin chaung, Nanpeit chaung and Nammeik chaung are typical for the drainage flowing from south to north, and also flowing into the Shweli river. Many streams criss-cross and help to drain the valley. The second drainage system start from the southern watershed of a rugged, hilly and mountainous region, flowing generally from northeast to southwest and from north to south, and then flowing into the Nampai chaung to Chaungmagyi river. Yini chaung, Nannga chaung, Nanat chaung, and Natpan chaung are good examples for the second system of drainage. Nampi chaung divides Mogok subdivision from the Mong-long.
The research will attempt to contribute the geology, mineralogy, petrology and mineralization of the igneous rocks of Mogok Stone Tract. The main objectives of this research are as follows:
- To study the distributions of the igneous rocks in the Mogok Stone Tract.
- To document the petrography, petrochemistry and petrogenesis (sequence and geochronology) of these igneous rocks.
- To investigate the gemstone deposits from these igneous rocks.
- Field Study
- Detailed geological mapping of the Mogok Stone Tract to investigate the structural and lithological features of igneous rocks.
- Systematic sampling of various igneous rock types.
- Gemstones sampling and to study the mode of occurrence of gemstones from igneous rocks of this research area.
- Laboratory Techniques
The representative samples of the research area were studied by means of the following techniques:
- Detailed microscopic examination of various igneous rocks for better understanding of the petrography of the area.
- Quantitative and qualitative elements analysis of various igneous rocks and minerals samples using the EDX-RF in URC, Yangon University and WDX-RF, LA ICP-MS techniques in University of Tasmania, Australia to contribute the petrochemistry and mineral chemistry.
- X-ray diffraction analyses of unknown minerals from these igneous rocks in X-RD Laboratory, Department of Atomic Energy.
- The radiometric dating of four samples of the area was analysed by U-Th-Pb geochronology method using LA ICP-MS and SHRIMP techniques at University of Tasmania, Australia.
- Some selected gemstone samples were identified by LRS (Laser Raman Spectroscopy) at University of Tasmania, Australia to contribute the solid/fluid inclusions in the corundum.
The Mogok Stone Tract has attracted many geologists, mineralogists and gemmologists from many parts of the world for producing the finest rubies on earth. Though rubies have been mined in Mogok for centuries, it remains unknown when these deposits were first discovered.
The earliest historical record is a description of the ruby mines at Mogok by Father Giuseppe d’Amato as reprinted, unedited, [by] the Journal of The Asiatic Society of Bangal, in 1833 (v. 2, pp. 75–76).
Brown and Judd (1896) reported mode of occurrence of the rocks and origin of gems, and firstly named the area as Mogok Stone Tract. Also they pointed out that the Mogok limestone, which [was] later named as marble, originated from the basic igneous rocks by means of complicated chemical reaction. They also considered the source of alumina in the corundum and spinel as the limestone itself.
La Touche (1913) reported the principal rock types of the Mogok Stone Tract and its environs; the term “Mogok Gneiss” as Archaen in age was firstly given by him, published in Memoirs of the Geological Survey of India, Northern Shan State, 1913. The arrangement of the geological succession is as follows:
Iyer (1953) contributed a valuable account of the geology and gemstones of the Mogok Stone Tract and mapped Mogok and its surrounding area, four-inches-to-one-mile; published in Memoirs of the Geological Survey of India, Volume 82, 1953 and arranged the geological succession of Mogok Stone Tract as follows:
- Recent Alluvium
- Pleistocene: Raised Terraces near Mogok and Mong-long
- Basic and Ultrabasic Intrusives: Dolerite, peridotite, hornblende-pyroxene rock and hornblende rocks. Hornblende and aegirine-scapolite rocks
- Urtite Series: Hornblende-nepheline rocks and aegirine-nepheline rocks
- Tourmaline Granite
- Kabaing Granite: Pegmatites, aplite, leptynite, minor intrusions, etc.
- Syenites: Nepheline syenite, etc.
- Augite and Hornblende Granites
- Quartzites: Quartz-sillimanite rocks of Nammi
- Calc-granulites: Scapolite-gneiss and pyroxene granulites
- Crystalline Limestones and Calciphyres (Rubies and Spinels): also bands of calc-gneiss
- Khondalites: Feldspathic garnet-sillimanite-gneisses with graphite and hybrid rocks
- Biotite-gneisses, Garnet-gneisses and Biotite-garnet gneisses: Highly injected with acid intrusives as pegmatites, feldspathic veins and quartz veins
He pointed out the origin of sapphire from Mogok as “the presence of sapphire in the pegmatite and granite in the Mogok area also presents as a case of supersaturation with alumina; and if this magma was supersaturated with alumina, this alumina must have been conveyed into the limestones by the agents of pneumatolysis.”
Searle and Ba Than Haq (1964) described the relationship of Mogok Belt to Himalayan Orogeny. They firstly explained the metamorphism of the Mogok Slone Tract took place in the Middle Tertiary and also they reported the rock type into groups. They are:
Myint Lwin Thein et al. (1990) studied the geology and stratigraphy of the metamorphosed early Paleozoic rocks of the Mogok-Thabeikkyin-Singu-Madaya areas. They correlated the metasediments of this area to the Lower Paleozoic carbonate-dominated sediments of the Southern Shan Slate, based on the macroscopic and megascopic lithologic similarities. They arranged the geological succession and the rock units in the present area as follows:
Also they described
ruby and sapphire regionally occurring in the Kyetsaung taung marble (a unit of Wabyudaung Marble) of this Mogok Belt is related to the fact that the Kyetsaung Taung marble is the host rock for the corundum mineral formation. This marble formation, like its unmetamorphic equivalent Wunbye Formation, with clayey or silty laminations, patches, or burrows was a carbonate unit rich in alumina. This rich alumina source, together with chromium content of the limestone after suffering from the high grade regional metamorphism caused by the granitic emplacement and several tectonism, was responsible for the formation of ruby. They further remarked that the occurrence of sapphire in syenite-alaskite might be accounted to the magma rich in alumina.
Thet Tin Nyunt (2000) studied the mineralogy and petrology of Bernard–Pyaung gaung area.
Thuzar Aung (2003) studied the petrology and gemstones of On-dan and its environs.
In addition, the various workers from universities also carried out the geological investigation, on the basis of their purposes, mainly concentrated on the gemmology, mineralogy, petrology and structural geology for their M.Sc., M.Res. and Ph.D. research.
|From the Pala International Corundum Collection. (Photo: Mia Dixon)|
Chapter II Geology of the Area
Mogok Stone Tract is a segment of the Mogok Metamorphic Belt (MMB) of Searle and Ba Than Haq (1964), and is situated south of the eastern Himalayan syntaxis at the western margin of the Shan-Thai terrane. This originated in Gondwana (Ridd, 1971) and collided with Asia either in the latest Triassic (Mitchell, 1977; Metcalfe, 1988) or earliest Triassic (Metcalfe, 2000). The study area, situated in the northern part of MMB has long been of great interest because of the rubies, sapphires and other gemstones. The geology of the Mogok area is very complex, consisting mainly of high-grade metamorphic schists and gneisses, igneous intrusives, including gem bearing pegmatites, peridot bearing ultramafic rocks, and most importantly ruby and spinel bearing marble. Generally, metamorphism, migmatization and structural deformation have involved metasediments, which range in age from Precambrian or Cambrian to possibly Cretaceous. Acid, intermediate, mafic to ultramafic igneous rocks form an integral part of the Mesozoic to Tertiary igneous unit.
The area is bounded in the north by east-west trending Momeik dextral fault (Sein Myint et al., 1979), Cretaceous Orbitolina bearing limestones which are intruded by gabbro and related rocks and older alluvial deposits are exposed. The boundary between the Tagaung-Myitkyina belt and the MMB is the high-angle Kyaukphyu fault, locally a southeast-dipping thrust (Mitchell et al., 2004). In the southern part of the area, Mong-long mica schist exposes a gneissic area intruded by tourmaline granite along the boundary. West of Mogok, Sagaing fault, major right-lateral strike-slip fault which is running north-south also dissecting Singu lava flow, and the western margin of the MMB is juxtaposed with late Tertiary sediments in the western portion.
[In] the southern part of the Mogok, Mong-long mica schist striking nearly east occupies a broad belt of the gneissic area and is intruded by tourmaline granite along the boundary with gneiss. The Mogok Stone Tract is bounded, as well as overthrusted, by the Chaung-Magyi Group in the southeast along the Chaung-Magyi stream, and tourmaline granite is emplaced along the thrust plane (La Touche, 1913). Among the imbricated thrust sequence, Mogok Thrust (Searle and Ba Than Haq, 1964) is the most distinct principal thrust fault in this area. The Kabaing Granite intruded into the area forming large exposure at Kabaing village traceable west towards the Thabeikkyin area.
|Click to enlarge.Regional geological map 0f the study area, modified after Bender (1983).|
|Regional geological map 0f the study area, modified after Bender (1983).|
On the basis of primarily field observations and petrographic data, and secondarily petrochemical and geochronological data, the geology and the rock sequence of the area are modified from some previous works (e.g. Iyer (1953), Myint Lwin Thein et al. (1990), Thet Tin Nyunt (2000), and Thuzar Aung (2003)). Three new geological maps were prepared for the Mogok–Kyat-pyin, Bernard–Pyaung-gaung and On-dan areas (Figs. 2.2, 2.3 and 2.4).
According to radiometric dating suggested that the age of leucogranite, syenite, Kabaing Granite, and pegmatite of the area. [Wording appears to be omitted from previous sentence. —Editor] However, the age of ultramafic rocks of the area are correlated with [the] eastern ophiolite belt of Myanmar (personal communication, Dr. Hla Htay, 2007). Field observations indicate that most of the igneous bodies in the area have intrusive contacts with the surrounding Mogok metamorphics or other igneous rocks.
Regarding the age of the latest regional metamorphism of the Mogok metamorphics, Maung Thein (2000), using some GIAC data, mentioned that the age of regional metamorphism along the Mogok Metamorphic Belt occurred in Late Oligocene. On the basis of some radiometric dating Bertrand et al. (2001) suggested that the age of metamorphism along the Mogok Metamorphic Belt ranged from Oligocene to Middle Miocene. However, it should be pointed out that Kabaing Granite (15–16 Ma) intruded into the Mogok metamorphics. Thus, the metamorphic age of the Mogok metamorphics would not range up to Middle Miocene.
|Major geological succession of the study area.|
The Mogok Stone Tract, composed [by] a variety of igneous rocks, ranges in composition from granite to peridotite. The probable igneous sequence in the area is contrived from the field relationships of some igneous rocks, and radiometric dating of some igneous rocks. These are shown in Table 2.1, and the field relationships are as follows:
Ultramafic rocks are relatively subordinate in the Bernard–Pyaung-gaung area, which are mostly intruded into the garnet-biotite gneiss (probably older than Mogok metamorphics). However, the biotite microgranite and the late stage of pegmatite are intruded into the peridotite at Pyaung-gaung, so these ultramafic rocks are generally older than biotite microgranite and pegmatite. It may be assumed that they have been emplaced to the garnet-biotite gneiss as early Jurassic?.
Recent field evidences indicate foliated and highly jointed augite-biotite granite (129.8±8.2 Ma). Early Cretaceous is intruded by leucogranite, which are foliated at the margin of the intrusion and trending nearly NE-SW at Taung-me Taung and Shwe-udaung Taung, the highest peak of Mogok area, showing that the foliated augite-biotite granite is older than the leucogranite (32±1 Ma) Early Oligocene in age.
Leucogranite occurs widespread as small stocks and dykes, which are intruded into regionally metamorphic rocks as well as syenite intruded into these rocks at Thurein taung. The contact relationship between leucogranite and biotite microgranite is absent in the study area. However, U/Pb zircon age of syenite is 25 Ma (Late Oligocene); it is younger than leucogranite. Also, some pegmatite dykes are intruded into the leucogranite at Dattaw and Pein-pyit area, indicating that the leucogranite is older than the pegmatite.
|Click to enlarge map.Geological map of Mogok–Kyat-pyin area, geology by Kyaw Thu, 2006.|
|Click to enlarge map.Geological map of Bernard–Pyaung-gaung area, modified after Thet Tin Nyunt (2000), Kyaw Thu (2006).|
|Click to enlarge map.Geological map of On-dan area, modified after Thuzar Aung (2003), Kyaw Thu (2006).|
Syenitic rocks and urtite series have intruded into the Mogok metamorphics in this area, as well as intruded into the leucogranite, i.e., syenite is younger than the leucogranite. But, biotite microgranite has intruded into the syenite in On-dan area, indicating that syenite is older than biotite microgranite (15.8±1.1 Ma) Middle Miocene.
The Kabaing Granite occupies a large tract of country to the NW of Mogok–Kyat-pyin area. It is intruded into the all Mogok metamorphic rock units and parts of the syenite, ultramafic and leucogranite. Unlike the augite-biotite granite, leucogranite, and syenite, the Kabaing Granite shows no signs of diastrophism and its emplacement post-dates that of the syenitic rocks. In Sakhan-gyi and Pan-taw, the Kabaing Granite is intruded by pegmatite dykes (15 Ma) Middle Miocene (Searle and Ba Than Haq, 1964) with trend of NNE-SSW in direction indicat[ing] that these pegmatites are younger than other igneous rocks.
Pegmatites and Alpites
The term pegmatite is a textural definition. The important pegmatite exposures [are] situated at Sakhan-gyi and Pan-taw, which are intruded into the Kabaing Granite. They usually occur as medium to very coarse-grained dykes, highly weathered and mostly kaolinized, whitish on fresh surfaces and brownish on weathered surfaces. The important gemstones and some rare gemstones are found in these pegmatites. Other pegmatites are also exposed at west of Pan-lin, Dattaw, Le-u and Pein-pyit area intruding the leucogranite and metamorphic rocks. Southeast of Pyaung-gaung area, the pegmatites are intruded into the peridotite and dunite. Minor aplite dykes and veins are also present in this area.
Kabaing Granite (biotite microgranite)
Kabaing Granite is one of the major intrusive igneous rocks in Mogok, and was first noticed by Brown and Judd (1896) near Kabaing on the motor road. This granite is a biotite granite, greyish, hard, compact and massive, medium-grained, homogeneous in texture, and regionally discordant to Mogok metamorphics. It occupies a vast area centered at Kabaing village, extending to Kyauk-pyat-that, turns northeast [to]wards Sawlone-gyi, and also extending to Kyauk-sin, Pan-taw and Injauk to Tam-saing and Laythar near Momeik boundary, where it is intruded into the Mogok metamorphic rock units. This microgranite is found at the southern and western part of On-dan village, which are intruded into the marble and leucogranite. Its southern boundary starts from Nam-sita chaung and passes under the quartzite south of Gwe-bin. This granite is also found north of Kathe, Kyauk-sin–Kyat-pyin road, north of Kyat-pyin view point and intruded into the marble north of Luda on the Mogok–Kyat-pyin road. It is also intruded into the garnet-biotite gneiss in Chin-the Taung and Hin-tha Taung slopes. The boundary of the Kabaing Granite and the country rocks [is] not very definite, as there is a thick cover of soil and [it is] heavily forested. Exfoliated or spheroidal weathered exposures are common in this area.
|Click to enlarge.(a) Highly weathered pegmatite exposure, Sakhan-gyi, 22° 54' 1.2" N, 96° 20' 56.1" E; (b) dyke of pegmatite at Pan-taw, 22° 57' 47.3" N, 96° 24' 15.6" E; (c) panoramic view of Kabaing Taung; inset: large block of biotite microgranite showing exfoliated nature at the peak, near Kabaing village; (d) small outcrop of Kabaing Granite showing onion skin weathering, 22° 57' 14.9" N, 96° 24' 54.6" E, Kyauk-sin–Pan-taw area; (e) an outcrop showing exfoliation nature in biotite microgranite, near On-dan village, 22° 57' 12.2" N, 96° 14' 38.05" E.|
Prof. Adams (1926) was the first to discover this suite of rocks on the Mogok motor road near view point to Sin-khwa. These rocks are mainly found in Kyauk-pyat-that, Myaing-gyi Taung, Thurein Taung, Sin-khwa and Ye-aye environ area, which are intruded into the marble and leucogranite, forming lenticular bodies, 10 cm to 20 cm in exposed width and at least 100 m in exposed length. These rocks show a gneissic banding nature, or are granulitic and vary in the amount of their salic and femic constituents. Other minor exposures of these rocks occur near Chaung-gyi, Injauk, south-east of Taung-me Taung and north-west of Bernard-myo (Ywa-thayar).
The syenitic rocks were first discovered in this area by Fermor (1932). These rocks are formed as sills or sheets, dykes and small stocks around the Mogok area. Syenite exposures are scattered or may cover vast areas and they may show foliation. This unit is found well developed in the area between Mogok and Taung-me Taung and around Let-nyo and Lay-thar Taungs. It is well seen as small stock between Taung-me–Mogok area, which is in contact with the marble. The rock occurs as dykes north of Ohn-gaing, Ye-bu, Dattaw chaung, Pein-pyit, Kyauk-wa, Achauk-taw, and Chaung-gyi chaung. Exfoliated syenite boulders are found near the village of Ma-nar and are locally called “ge-sein” (in Myanmar, green rock).
|Click to enlarge.(a) Phlogopite-diopside marble and urtite rocks contact in Thurein Taung, 22° 54' 12.2" N, 96° 22' 18.8" E; urtite exposure showing highly brecciated nature due to fault contact nature (inset); (b) urtite and white marble contact in Yadana-kadae-kadar mine, 22° 54' 34" N, 96° 22' 31" E; mafic minerals mainly hornblende and nepheline in surface of urtite exposure (inset); (c) urtite intruded into the marble showing scapolite-diopside-graphite contact zone, 22° 54' 11.3" N, 96° 22' 17.3" E; (d) pegmatite vein intruded into the urtite body, Thurein Taung, 22° 54' 12.4" N, 96° 22' 20.6" E; (e) xenolith of nepheline syenite in urtite, Thurein Taung, 22° 54' 12.7" N, 96° 22' 20.7" E.|
|Click to enlarge.(a) A distinct syenitic rocks exposure showing exfoliated nature in syenite exposure, north of Ohn-gaing village, 22° 56' 27.2" N, 96° 29' 36.8" E; (b) syenite exposure at Kyauk-wa, north of Mogok; (c) dyke of urtite in syenite exposure, north of On-dan, 22° 57' 16.4" N, 96° 14' 39" E.|
Bernard-myo exposure is the next largest one, which is well exposed at the southwest and northern part of Bernard-myo. Small exposures are found at the southern part of Pyaung-gaung village and east of Pan-lin village. It extends as the minor bands on to the Kyauk-thita Taung and north-east of Injauk. Other smaller exposures are also present.
Other exposures are found at the Kyat-pyin environs, such as east of Kyauknaga, north-east and west of Tha-dut-sho and north of Pyaung-pyin, and north-east of Baw-Ion-gyi, Kyauk-sin, and Baw-ma. Exposures of syenitic rocks are also found as small stock and dykes around Pin-gu Taung, Kyauk-pyat-that, and Thurein Taung, Gegyi Taung, and northwest of On-dan village associated with leucogranite. A few small exposures of the syenitic rocks are also observed in this study area closely associated with the Mogok marble as a result of ruby formation by contact metamorphism.
These rocks were previously described as “Alaskite Suite” by Searle and Haq (1964), later renamed by Myint Lwin Thein et al. (1990) as “Pingu Taung Leucogranite.” Leucogranite constitutes the major part of the igneous rocks found in the Mogok Stone Tract, which intruded into Mogok metamorphic rocks and it appears highly weathered, showing pronounced exfoliation with graphic texture and foliation.
Between Mogok and Kyat-pyin, these rocks are found in the west of Pein-pyit, south, south-west and north-east of Dattaw Taung, east and north-east of Le-u. This unit crops out as an intrusive mass around the peak of Kyauk-taung-kon, Myo Taung, Chin-the Taung, and as small bodies in Ye-aye valley, and also at the base of western and northern spur of Pingu Taung, extended along the foot path between Baw-Ion-gyi and Baw-mar, and at the Gwe-bin chaung near the Kyauk-pya village. These leucogranites are closely related to the syenitic rocks, and probably important source rocks for radioactive minerals in Mogok.
In the Bernard-myo area, it is the most abundant igneous rock and mainly found in the western part of Pan-lin and Ye-ne-inn villages, which are intruded into the garnet-biotite gneiss and calc-silicate rocks. In the southern part of Htin-shu Taung, leucogranite intruded into the marble and shows foliated nature.
Leucogranite occurs as the largest intrusive mass in the On-dan area, typically found in Pa-Iaung Tung, Hnama-taw-Iay range, at the base of Tant-khan Taung to [the] western part of On-dan village. These rocks are closely associated with Mogok metamorphic rocks as well as syenite and augite-biotite granite in this area.
|Click to enlarge.(a) A distinct exposure of leucogranite in Hin-thar Taung; (b) photograph showing leucogranite and diopside-phlogopite marble contact to form the painite deposit in Wet-loo mine, 22° 54' 28.5" N, 96° 23' 34.9" E; (c) highly weathered leucogranite exposed in Saw-mar mine; (d) an outcrop showing exfoliated nature in leucogranite, north of Saw-mar; (e) photograph showing leucogranite intruded into the garnet-biotite gneiss in Pan-taw, 22° 57' 44.6" N, 96° 24' 41.7" E; (f) syenite vein in leucogranite about three feet in thickness, Wet-loo mine, 22° 54' 28" N, 96° 23' 35" E.|
The main intrusions are along the Shwe-u-daung Taung range, north of On-dan village and Taung-me Taung peak, north of Mogok respectively. In On-dan, augite-biotite granite is found intruded by leucogranite in some outcrops. It shows strong foliation on weathered surfaces, similar to ridge and furrow structure. Other small exposures occur in the area such as Kyauk-sin and Saw-mar, which are very similar in weathering effect to the syenitic rocks, [and] represent their more acid phase.
Ultramafic and Mafic Rocks
Ultramafic rocks of the Mogok Stone Tract occur as layered intrusions in garnet-biotite gneiss (probably older than Mogok metamorphics) in Bernard–Pyaung-gaung area, north-eastern part of the Mogok. These rocks are distinctly cropped out at the Pyaung-gaung, Zalat Taung, Mya-sein Taung, Thit-ta-pin Taung, and Htin-shu Taung environs. Rarely, amphibolite and micaite rocks are also encountered in this area. Smaller bodies of biotite microgranite, feldspathic veins and veinlets of chrysoprase are also found intruded in these peridotite-dunite.
The mafic rocks, mainly gabbro, occur as small bodies in the surrounding area of Kyauk-pyat-that, environs of Ye-aye, Injauk and north-west of Tam-saing, which are not always large enough to be mapped.
|From the collection of Bill Larson. (Photo: Mia Dixon)|
2.4 Geological Structures
According to the TM image and photogeological interpretation, the study area is very complex in geological structure. [The] general trend of the rocks of Mogok area is distinctly in ENE-WSW direction and generally steeply inclined towards southeast direction. Numerous folds, faults and joints are involved. This area lies in a series of continuous and discontinuous anticlinal ridges and south-plunging synclinal valleys extending laterally from Kyini Taung to Kabaing, [and] marble and calc-silicate rocks are widespread throughout in this regional fold pattern.
|Click to enlarge.(a) Panoramic view of the peridolite-dunite bodies, north-east of Bernard-myo; (b) peridotite exposure showing false bedded nature, Mya-sein Taung, 23° 00' 03.4" N, 96° 27' 54.4" E; (c) photograph showing peridotite partly altered to serpentinite due to the auto metamorphism, 22° 59' 55" N, 96° 27' 46.6" E; (d) an outcrop showing jointed nature in dunite, Pyaung-gaung, 23° 00' 40.5" N, 96° 26' 40.0" E; (e) pegmatite dyke in peridotite and chrysoprase veins in upper part of photo, Mya-sein Taung, 23° 00' 10.5" N, 96° 27' 44.9" E.|
|Click to enlarge.(a) Panoramic scenery of Taung-me Taung; augite-biotite granite exposure at the peak of Taung-me Taung (inset), 22° 58' 18.4" N, 96° 28' 8.5" E; (b) augite-biotite granite exposure showing the distinct faulted nature in Shwe-u-daung Taung; inset; small quartzo feldspathic vein cross cut in foliated augite-biotite granite, north of On-dan village, 23° 01' 12.1" N, 96° 13' 19.07" E.|
[An]other distinct feature is the Mogok thrust, generally NE-SW trending and which follows a sinuous outcrop from the head of Mogok valley to southwest of Gwebin village; however, the appearance of the thrust between Mogok and Kyat-pyin is vague by the high accumulation of faulting, and some forceful emplacement of leucogranite. Deformation, as being the equivalent of local stretching of crustal material around the eastern Indian syntaxis, [was] active between Oligocene and Middle Miocene (Bertrand et aI., 2001). At the Latitude of [the] Mogok area, the deformation was sealed at about 16 Ma (Middle Miocene) by intrusion of the Kabaing Granite.
|Click to enlarge.(a) Photograph showing mullion structure in calc-silicate rock due to the thrusting, east of Gwe-bin, 22° 53' 44" N, 96° 22' 24" E; (b) dyke of urtite showing folded nature in marble indicating tectonism effect, Kyauk-saung, 22° 55' 21" N, 96° 25' 53" E; (c) the exposure showing Mogok thrust, north-west directed thrust plane at north of Mogok, 22° 56' 37.5" N, 96° 31' 22" E; (d) close-up view of photo (c) showing footwall carbonate mylonite along the thrust zone; (e) well jointed nature in phlogopite marble at Gwe-bin.|
Thus conclude Chapters I and II. Access Chapter III here.
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