Early Stage of Burmese-Malayan Geosyncline.pdf

Geol. Soc. Malaysia, Bulletin 6, July 1973; pp. 119-129.

The Early Stage of the Burmese-Malayan Geosyncline

TEll CHI KOBAYASHI1

Abstract: The history of this geosyncline is divided into three stages: (1) Devonian and older ; (2) late Devonian to middle Triassic; and (3) la ter Mesozoic period. The so­called Pre-Cambrian metamorphic rocks require a further confirmation of their ages Upper Cambrian is the oldest dated sediment of the geosyncline. Three facies named Shihtien, Naungkangyi, and Thungson, can be distinguished in the Ordovician formation. In the later Palaeozoic sequence carbonate-rich and carbonate-poor facies alternate twice or more with intercalations of graptolites and tentaculites facies and other clastic facies . Broadly speaking, the early stage was the age of epirogenic undulations, while the second stage was the age of embryonic foldings by which the geosyncline was partly modified, and at length it was wholly deformed and consolidated by Mesozoic orogenies.

INTRODUCTION

During the Palaeozoic Era the Burmese-Malayan geosyncline extended from the Shan Plateau and west Yunnan in the north to the Thai-Malayan Peninsula in the south and further into Borneo. In this sedimentary zone Ordovician cystoids have already been reported from Burma by Noetling (1890), and in west Yunnan by Loczy, (1898). Subsequently the Palaeozoic biostratigraphy had been greatly clarified by La Touche (1913), Coggin Brown, Sondhi, Reed, Yin, Lu and others, till at length Cambrian trilobites were discovered in the Paoshan area, west Yunnan by Sun (1938). Then, schematizing the Palaeozoic sequence, he called this trough the "Sino-Burmese geosyncline". (Sun, 1945, p. 48).

In the Thai-Malayan Peninsula a Carboniferous fauna was first described from Phattalung by Reed (1920), but for a long time little was known of the older history (Alexander, 1956). In the last 15 years, however, all of the Palaeozoic Systems were documented by fossil evidence in the southern area of this zone. Therefore, the "Sino-Burmese-Thailand-Malayan geosyncline" was abbreviated to the "Burmese­Malayan geosyncline" (Kobayashi, 1964).

In my opinion it is relevant to divide the history of its development into three stages. Main events in the early stage were wide and gentle movements of the geo­syncline, causing oscillations of shore line in the Devonian and older periods as revealed in the gradual variations of sedimentation and local discordances. In the middle stage, from late Devonian to middle Triassic, local crustal disturbances and igneous activities took place, but they were not strong enough to change the principal outline of the geosyncline. During the Mesozoic Era, however, the geosyncline suffered strong orogenic activity accompanied by the emplacement of granites through which the whole geosyncline has become emergent and consolidated.

CAMBRIAN SEDIMENTS AND THE SO-CALLED PRECAMBRIAN ROCKS

Upper Cambrian trilobites occur in shales at Paoshan and Mangshih, west Yunnan, in the north, and in the Tarutao sandstone at Tarutao island just to the north of the Thailand-Malaysian boundary (Sun, 1939, Kobayashi, 1957, Lu, 1964). In the Langkawi Islands to the south of the boundary the thick "Machinchang

1 Geological Institute, University of Tokyo, Tokyo (Hongo), Japan.

120 TEIIeRI KOBAYASHI

clastic series" is overlain by fossiliferous Ordovician limestone, but its base is un­exposed (Jones, 1968).

In Thailand, the "Phuket series" was ascribed to the Cambrian by the inclusion of Planulites( ?) (Brown et al. (1951), but such an impression is not a reliable Lower Cambrian indicator (Kobayashi, 1960). Toriyama and others (in Kobayashi et al., 1964) referred it to the "Kanchanaburi series" in view of the fact that it was located beneath the Permian Rat Buri limestone and that fenestellids and other fossils in its pebbly sandstone were suggestive of Carboniferous. Recently Young and Jantaranipa (1970) reached the same conclusion when they found Waribole perlisense below the Bryozoan beds. The "Kanchanaburi series" or Tanaosi group (Javanaphet, 1969) extends down as far as Lower Devonian because it contains Plagiolaria, mono­graptids, and tentaculitids (Kobayashi and Hamada, 1968).

In the Shan States the "Bawdwin volcanic series", which rests on the metamor­phosed "Chaung Magyi series" unconformably, is conformably overlain by the Ordo­vician Naungkangyi beds with the Pangyun sandstones and grits at the passage beds. If the rhyolite lava flow, tuff, and agglomerate of the series are really Cambrian in age, the Bawdwin volcanism is an exceptional event in Eastern and Southeastern Asia.

In the correlation Tables of China, Supplement, (Compilation Committee, etc., 1958), it is shown that the basement complex of west Yunnan composed of the Tsangshan gneiss and Shihku schists is overlain by the pre-Cambrian Kaoliang phyllite, shale, and quartzite formation, and the latter in turn by the Upper Cam­brian Paoshan series, both unconformably. According to Sun and Szetu (1947), however, the Archaean Tsangshan gneiss complex is in thrust contact with meta­morphosed Ordovician rocks in the Paoshan area. The so-called Kaoliang rocks are there metamorphosed Palaeozoic and Triassic ones. The Kaoliang series is absent in the Tali-Liukiang area, west Yunnan.

In north Thailand the Precambrian gneiss series appears to be overlain by the less metamorphosed Cambrian-Ordovician formations, but "an undisturbed trans­gressive contact between Precambrian and Palaeozoic rock has not yet been ob­served." (Baum et al., 1970).

In west Malaysia are Kelantan schists, Taku schists and the like whose Precam­brian age was a debatable subject (Hutchison, 1961; Alexander et al., 1961). Re­markably enough Ladinic Daonella and Paratrachyceras(?) are contained in a green schist in south Kelantan which deserved regional metamorphism (Kobayashi et aT., 1967).

Little is actually known of the basement of the geosyncline. Much uncertainty remains about the so-called Precambrian rocks. It is however, certain that there was a long trough extending from the Sino-Burmese borderland to the Thai-Malayan peninsula already in the late Cambrian Period.

THREE FACIES OF ORDOVICIAN SEDIMENTS

The Ordovician sediments and faunas of the geosyncline can be classified into the following three facies:

THE EARLY STAGE OF THE BURMESE-MALAYAN GEOSYNCLINE 121

1. The Shihtien * facies, chiefly composed of shale and limestone and rich in grapto­lites, but also containing various shelly fossils in the middle and upper parts. Three formations and six zones are distinguished in the Ordovician system of the Paoshan area, four of which are graptolite zones (Sun & Szetu, 1947). How far graptolites are distributed southward is an important question, because the Paoshan facies indicates the axial zone of the geosyncline in the Ordovician period.

2. The Naungkangyi facies is composed of shale, marl, and limestone, and contains various fossils, although graptolites are rare. A wealth of cystoids is a charac­teristic which this and the preceding facies have in common. The typical display of this facies is seen in the northern Shan states, but it is widespread also in the southern Shan states.

3. The Thungsong limestone facies containing shelly faunas at Thung Song and Satun in Thailand, and in Perlis, Perak, and especially in the Langkawi Islands in Malaysia. The Thungsong faunas comprise various fossils at different hori­zons, but graptolites and cystoids are as yet unknown. Three conodont zonules are distinguished in it by Igo and Koike (1967, 68). Teiichispira and Discoceras (Hardomanoceras ?) suggest an upper Canadian-lower Chazyan and actino­ceroids, brachiopods and some others are Mohawkian (Kobayashi, 1958, 1959; Kobayashi & Hamada, 1963 ; Hamada, 1963 ; Yochelson & Jones, 1968). This and the preceding facies are linked with Armenoceras and Ormoceras from the Huai Urn Lu, Northwest Thailand (Kobayashi, 1961), nautiloids from Kyaukse (Thein, 1968), and the Orthoceras beds near Mawson, south Shan states (Reed, 1936).

Noteworthy is the Tambak mudstone (Kobayashi and Hamada, 1970, of the lower Mahang formation in central Perak in which Microparia is abundant beside graptolites and some other fossils as it is the southern member of the Shihtien facies.

MIDDLE PALAEOZOIC SEDIMENTS

Broadly speaking, the later Palaeozoic sediments of the geosyncline may be classified into the carbonate-rich and carbonate-poor facies which alternate twice, as below.

(5) Upper Plateau limestone, Permo-Carboniferous.

(4) Lower dolomitic Plateau limestone, Middle and Upper Devonian.

(3) Zebingyi beds and other tentaculites beds, Middle Silurian-Middle Devonian.

(2) Kuala Lumpur limestone and its equivalents, Middle and Upper Silurian.

0) Panghsapye beds and allied graptolite beds, Lower Silurian.

Silurian The Panghsapye facies is represented by the lower Jenhochiao series in west

Yunnan, Panghsapye beds in the Shan states, Llandoverian graptolite shales in North-

*Paoshan facies (Kobayashi in Abstracts of Papers. 1972) is better replaced by Shihtien facies as the former is easily confused with the Upper Cambrian Paoshan Series.

122 TElIeRI KOBA Y ASRI

west Thailand (Bastin et al., 1970), the so-called Lower Detrital band of Pulau Lang­gon (Jones, 1961), and Llandoverian graptolite shales of the Mahang formation in Malaysia (Burton, 1971). Dalmanitina occurs in the basal parts of the band and in the Panghsapye beds (Reed, 1915, Kobayashi and Hamada, 1963, Kobayashi et ai. , 1963). Thus the graptolite-bearing Llandoverian was widespread in the geosyncline, overlying the Ordovician.

In the Langkawi islands the Lower Detrital band is intercalated between the lower and upper Setul limestones containing conodonts in many horizons (Igo and Koike, 1967, 1968) and the rich Prodontochile fauna in the basal part of the upper Setullimestone whose age is late Llandoverian, if not early Wenlockian (Kobayashi and Hamada, 1971). In the Kanthan area, Perak, Upper Ordovician and Silurian corals occur respectively below and above a wedge of graptolitic shales (Thomas & Scrutton, 1970). The Kuala Lumpur Limestone in Selangor yields Middle and Upper Silurian corals, brachiopods, gastropods, and crinoids (Thomas, 1964; Gobbett, 1964 ; Boucot, Johnson & Jones, 1966). In northwest Thailand many Ludlovian conodonts were found in limestones intercalated in clastic series (Bastin et al., 1970).

In west Yunnan, the upper Jenhochiao series is mainly composed of limestones and contains Wenlockian corals and other fossils. In east Burma, the Namhsim beds consist of the Namhsim sandstone in the lower and the Konghsa marl in the upper part, both yielding various Wenlockian fossils .

It is a general tendency for limestones to be developed more in the Wenlockian than the Ludlovian and more in the south than in the north, while the Devonian and Anthracolithic carbonates were developed more and longer in the north than the other, seeing that the Moulmein and Rat Buri limestones tend to thin out southwards.

Devonian The sedimentation of the tentaculites facies cont-inued in the geosyncline from

Silurian to Devonian but the carbonate facies became predominant from late Middle Devonian . In the Sino- Burmese borderland the former is represented by the Washih and Zebingyi formations. The latter consists of the lower part of the Plateau limestone in the Shan states and the Hoyuanchai formation in west Yunnan. They are built up with dolomitic limestone in main and contain the Eifelian Padaukpin fauna in reef limestone, the Middle Devonian Wetwin fauna in shale intercalation (Reed, 1908, Anderson et al., 1969), and the Frasnian fauna near Padaukpin (Reed, 1930). Stringo­cephalus and CyrtospiriJer l'erneuili indicate the Givetian and Famennian age respec­tively in west Yunnan.

In northwest and west Thailand the Lower Devonian and (7) Eifelian are docu­mented by graptolites, tentaculites, conodonts and other fossils, and the Givetian and Upper Devonian by conodonts (Jaeger et ai. , 1968, 1969; Bastin et al., 1970). In Malaysia, Lower Devonian monograptids are widely distributed in the Upper Detrital band of Pulau Langgon , the Mahang Formation in Kedah and Perak and the Foothills formation in west Pahang (Jones , 1967, 1970). These monograptids are often accompanied by tentaculites (Burton, 1967). Recently monograptids of the hercynicus group were found near Maymyo, northern Shan states (Berry in Muller, 1967).

In Penins.ular Thailand Plagiolaria and monograptids are contained in the tenta­culites shales of the Kanchanaburi series between Trang and Phattalung (Kobayashi

THE EARLY STAGE OF THE BURMESE-MALAYAN GEOSYNCLINE 123

and Hamada, 1968). In Upper Perak a unique Devonian fauna was found at Kroh in a tentaculites-bearing silty mudstone bed of the Baling Formation. It contains Plagiolaria. Most of the Kroh brachiopods are dwarfed. Pseudotrinodus is an isolated relic genus of the Agnostida. Because the visual organs are degenerated in the Kroh trilobites, their habitat would have been a deep and dark shelter and stagnant water there was unfavourable for benthos (Kobayashi and Hamada, 1971).

Givetian Stringocephalus was found in a limestone at Kampar near Ipoh, Perak (Gobbett, 1966). Middle and Upper Devonian conodonts are contained in limestones near Ipoh (Alexander and Muller, 1963; Muller, 1967). Heliolites and Clathrodictyon from the Danau formation, Borneo, show that the geosyncline was extending into central Borneo from the Malayan peninsula (Rutten , 1943).

Finally, there is a red shale formation in Northwest Malaya which contains Waribole perlisense, ambocoeliids and others (Kobayashi and Hamada, 1966; Ha­mada, 1968, 1969, 1970). The age of the fauna is Upper Devonian and/or Lower Carboniferous. The distribution of this red formation must be very extensive, because ambocoeliids of the same age occur in north Thailand (Hamada, 1968).

PALAEOZOIC CRUSTAL MOVEMENTS AND IGNEOUS ACTIVITIES

The discordance between the Naungkangyi beds and the Chaung Magyi series show the Ordovician transgression . Those at the base of the Namhsim sandstone on the Ordovician Hwe Maung and older sediments, the Konghsa marl on the Naung­kangyi beds, the Zebingyi beds on the lowest Silurian Nyaungbaw limestone, and the Plateau limestone on the Naungkangyi beds, reveal local deformations and major and minor transgressions in the Silurian-Devonian times, causing oscillations of the northwestern shore line of the trough. Granites, vein-quarts and other older rocks contained in the basal part of the Namhsim sandstone, pebbly sandstone of the Phuket series and conglomerates of the Mergui series in lower Burma must have been derived from the land on the west side of the geosyncline. Incidentally, the Mogok gneiss belt is now considered a product of repeated intrusions of granites from Precambrian to Cretaceous (Searl and Haq, 1964).

Koopmans (1965) postulated a folding phase in late Silurian to Devonian times from the mode of deformation of the Cambrian, Ordovician , and Silurian, formations and intruding granite sills in northwest Malaya, and proposed "Langkawi folding phase" for it. He emphasized the lack of Devonian strata in Thailand and the pre­sence of only a few patches of Middle-Upper Devonian in Malaya as indications of the phase. The Devonian system is , however, known now to be extensive in Thailand and Malaysia. The Upper Silurian and Lower and Middle Devonian formations are continuous and often combined in the tentaculites facies. There is no extensive hiatus or non-deposition at Ludlovian as claimed by Burton (1967).

In Pulau Langgon, Langkawi Islands, the Upper Detrital band, Lower and Middle Devonian in age, is unconformably overlain by the conglomeratic mudstone at the base of the red beds (Kimura and Jones , 1957). According to Jones (1968) the Upper Devonian to Lower Permian Singa and Kampong Sena formations overlie the Lower Devonian and older Palaeozoic unconformably in the northwestern part of the Malayan peninsula, but the discordance becomes indistinct easterly and the Middle Palaeozoic limestone is unbroken in central Perak.

Burton (1966) argued for the existence of the Langkawi folding phase, saying that it "is most probably of Middle to Upper Carboniferous date," because granite

124 TEIICH! KOBAYASHI

detritus and fragments of metamorphosed argillites are contained in the Singa and Kampong Sena formations. He considered that it constituted the culmination of a clearly defined Upper Cambrian to Lower Carboniferous cycle of sedimentation. Now, however, it is known that the sequence of these periods reveals polycyclic alternations of carbonate and clastic facies , instead of a simple grand monocycle.

Brown and others (1951) have already pointed out that in Thailand "The massive Rat Buri limestone in many places lies at flatter angles than the underlying beds suggesting either that the limestone was deposited nonconformably on the intensely folded Paleozoic sedimentary rocks or that the limestone was thrust up over them." Martini (1950) supported the latter alternative, considering that the apparent dis­cordance may be due to differential deformation between the limestone and the underlying incompetent rocks.

Recently Baum and his co-workers (1970) divided the Carboniferous orogeny in north Thailand into three phases, namely: (1) early Lower Carboniferous move­ment accompanied by granite intrusion; (2) Middle Carboniferous basic volcanism and (3) early Upper Carboniferous movement and ensuing intermediate and acidic volcanism. The inclusion of reworked fragments of Lower Palaeozoic rocks in the Lower Carboniferous sandstone is a proof for the first phase. The third phase is verified by the direct superposition of the Upper Carboniferous conglomerates on granite. In addition it is noted that the early Triassic movements are evidenced by conglomerates, especially in the region west of Mae Seriang.

In the Malayan Peninsula in the south, the Pahang volcanic series represents the intrageosynclinal volcanism in the Carboniferous-Triassic periods which was widespread in Pahang, Kelantan, Trengganu , Johore and other states (Alexander, 1956).

In the Shan plateau in the north Brunnschweiler (1970) split the Plateau limestone into the Devonian Shan dolomite and the Permian Tanbo limestone at the Carboni­ferous break. Such a break is, however, probably local because the contemporaneous sequence in west Yunnan consists of the Devonian Hoyuanchai dolomitic limestone, Dinantian Fengning series, Moscovian Huanglung limestone, Uralian Maping series, Permian Chihsia and Maokou limestones and the Upper Permian Heinishao series, all fossiliferous. The Plateau limestone extends into the lower Triassic at Hsenwi, Burma (Salmi, 1931). There was no volcanism in this part of the geosyncline, although the distribution of the Permian Omeishan basalt extends to a part of Yunnan from Szechuan.

It is reported that the so-called Kumming movement broke out in Yunnan and Indochina, but little is known of the phase of deformation in west Yunnan. The effect of these movements on the geosyncline is not yet known precisely.

The appearance of the red beds and the discordance at the beds mark off the beginning of the Middle stage of the Burmese-Malayan geosyncline. In the early stage there occurred no orogenic movement, although some intrageosynclinal vol­canism in the late Ordovician and late Silurian times is reported from the Malayan peninsula. (Jones, 1968).

Because this is a synthetic study, a relatively long bibliography is here appended to show the source of data, particularly recent papers on the geology of Thailand and West Malaysia.

THE EARLY STAGE OF THE BURMESE-MALAYAN GEOSYNCLINE 125

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ANDERSON, M.M., BOUCOT, A.J. and JOHNSON, J.G. (1969) . Eifelian Brachiopods from Padaukpin, Northern Shan States, Burma. Bill!. British Mus. (Nat. Hist.) Geol. vol. 18, no. 4, pp. 108-163, 10 pIs, 10 figs.

BASTIN, H., BRAUN, E. v., H ESS, A., KOCH, K .E., STEIN, V., STOPPEL, D. and WOLFART, R. (1970) . Silurian and Early Devonian Biostratigraphy in Northwest Thailand. Newsl. Stratigr. vol. I, no. 2, pp. 25-32, 1 fig. 2 tabs.

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---- , and KOCH, K.E. (1968). Ein Beitrag zur stratigraphischen Neuordnung des Palaozoi­kum in Sud-Thailand. Geol. Jahrb . 86, pp. 879-884, I fig.

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BROWN, J.e. (1950). Contributions to the Geology of the province of Yunnan in western China, 11. The regional relationships of the Ordovician. faunas. Rec. Geol. S{(rv. India, vol. 81, pp. 321-376, 2 tabs.

----, and SONDHI, V.P. (1933). Geological reconnaissance in the Southern Shan States . Ibid. vol. 67, pp. 135-165.

---- and (1933). The geology of the country between Kalaw and Tungyi, Southern Shan States. Ibid. vol. 67, pp. 166- 248 .

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BURTON, e.K. (1966). Palaeozoic Orogeny in North-west Malaya. Geol. Mag. vol. 103, pp. 364-365.

---- , (1967). Dacryoconarid Tentaculites in the Mid-Palaeozic Euxinic Facies of the Malayan Geosyncline. JOllr. Pal. vol. 41, no. 2, pp. 449---454, 3 figs.

---- (1967), Gra ptolite and Tentaculites Correlation and Palaeogeography of the Silurian and Devonian in the Yunnan-Ma layan Geosyncline. TrailS . Proc. Palaeollt. Soc. Japan, N.S. No. 65, pp. 27---46, I fig . 4 tabs.

- --- (1967). The Mahang Formation: a mid-Palaeozoic Euxinic Facies from Malaya-with Notes on its Conditions of Deposition and Palaeogeography. Geol. en MijnboulV, 46e, Jaarg. nr. 5, pp . 167- 187, 13 pis, 3 figs. 4 tabs .

- --- (1970). Lower Palaeozoic Rocks of Malay Peninsula: Discussion. Am. Ass. Petrol. Geol. BIIIl. vol. 54, 110. 2, pp. 357-360.

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CHIBBER, H.L. (1934). Geology of Burma, 538 pp. 37 figs, 23 pIs, 3 geo!. maps, Macmillan .

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CLEGG, E .L.G. (1954). The Mergui , Mou lmein and Mawch i Series with a note in the evidence for the Permian age of the Moulmein system by H .B. WHITIINGTON . Rec. Geol. Surv. India, vol. 78, pt. 2, pp. 157- 194, 2 pIs, 1 geol map.

COMPILATION COMMlTIEE FOR GEOLOGY OF CHINA AND GEOLOGI CAL INSTITUTE, ACADEMIA SINICA (1958). Regional Stratigraphic Tables of China. Supplementary Volume, 190 pp. 1 fig .

GOBBETI, D.J. (1964) . The Lower Pa laeozoic R ocks of Kuala Lumpur, Malaysia. Federation Mus. Jour . vol. 9, N.s., pp. 67-79, 3 pis. 2 figs. 2 tabs.

---- (1966). The brachiopod genus Slringocephalus from Ma laya. JOUY. Pal. vol. 40, pp . 1345-1348, 1 pI. 3 figs.

HAMADA, T. (1963). Some Midd le Ordovician Brachiopods from Satun , Southern Thai land. Japan. Jour. Geol. Geogr. vol. 35; pp. 213-221, pI. 10; Geol. Palaeont. S.E. Asia, vol. 1, 1964, pp. 279-287, 1 p I.

---- (1967). D evonia n of East Asia. Intern. Symp. o n Devon. System. Calgary, 1967, vo l. I , pp. 583-596, 6 figs.

(1968). Swaicoelia, a new Ambocoeliid genus (Brachio poda) from North T hailand . Geol. Pal. SE. Asia, vol. 5, pp. 1- 11 , 1 pI. 3 figs.

---- (1968). Ambocoeliids from Red Beds in the Malayan pen insula . Ibid. vol. 5, pp. 13-25, 1 pI. 7 figs.

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---- (1970). D evonian Brachiopods from Jpoh, Upper Perak in Malaysia (Ma laya) ibid. vol. 7, pp. 1-13, 2 pis, 1 fig.

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----, STEI " V. and WOLFART, R . (1969). Fauna (Graptoliten, Brachiopoden) del' unter­devonischen Schwarzschiefer Nord-Thailands, mit einem Beitrag von D . STOPPEL. Neues Jahrb. Abh. Bd. 133, HIt. 2, pp. 728-730, 1 fig.

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JONES, C .R. (1967). Graptol ites of the Monograptus hercYllicus type recorded from Malaya. Nature vol. 215, no. 51000, p. 497.

---- (1968). Lower Palaeozoic rocks of Malay Pen insula. Am. Ass. Petrol. Geol. Bull. vol. 52, 110 . 7, pp. 1259-1278, 5 fi gs.

---- (1970). On a Lower Devonian Fauna from Pahang, West Ma lays ia. Bul!. No.3, Geol. Soc. Malaysia , pp . 63-74, 1 pI. 1 fig . 1 tab.

----, GOBBETI, D.J. and KOBAYASHI, T. (1966). Summary of Fossil Record in Malaya a nd Singa pore. Geol. Pal. SE Asia, vol. 2, pp. 301-359. 9 ta bs. 1 map. Un iv. of Tokyo Press.

KIMURA, T. and JONES, e.R. (1967). Geologic Structu re in the northwestern and southern pa rt s of the Langkawi Islands, Northwest Malaysia. Geol. Pal. SE. Asia, vol. 3, pp. 123-134, 8 figs .

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KOBAYASHI , T. (1957). Upper Cambrian Fossils from Peninsula Thai la nd. Jour. Fac. Sci. Univ. Tokyo, sec. 2, vol. 10, pt. 3, pp. 367-382, p is. 4-5.

---- (1958). Geology of T ha iland and her Surroundings. JOllr . Geogr . Tokyo, vol. 67, no. 4, pp. 171- 188, 7 figs .

THE EARLY STAG E OF THE BURMESE-MALAYAN G EOSYNCLINE 127

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