ISSN 0866 - 7381

Journal of

SPECIAL ISSUE

No 7-8

Se ries B
1996

TpPR
COCEEDINGSOFTHEINTERNATIONALSVTVIPOSIUM
PR
GEOLOGY OFSOUTHEAST ASIA
ANDADJACENT AREAS

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UNESi

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32

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1- 9November 1995, Hanoi

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GEOLOGICAL SURVEYOF VIETNAM
HANOI


Journal of GEOLOGY
Series B, No.7-8/1996
Thirty sixth year

E D IT O R IA L O F F IC E

6 Phạ m Ngũ Lão, Hà Nộ i
Tel: 84. 4.8 ( 253 110, 246 461, 352319)
Fax 84.4. 8 254 734

EDITORIAL BOARD
Editor - in - chief: TRAN VAN TRỊ
Members: LÊ ĐỨ T AN, LÊ VAN TRẢ Ọ , NGUYEN GIAO, NGUYEN KHẮ C VINH, NGUYEN
NGHIÊM MINH, NGUYỄ N TIEN THÀNH, NGIJYEN TRỌ NG YÊM, NCHJYEN x u â n b a o , p h ạ m v ầ n
AN, PHAN C ự TIẾ N, PHAN TRUỜ NC. TIIỊ ,TÀNG MlJỜ I,Tổ NG DIJY TILANII,TRẰ N MINH THẾ ,
VÕ CƠNG NGHIỆ P, VŨ KHÍJC ( Deputy Hditor - in - chief),v ũ NGỌ C HẢ
I (Deputy Editor - ill - chief),
Secretary: BÙI Đ ÍJt THẢ NG

CONTENTS
PROCEEDINGS OF THE INTERNATIONAL SYMPOSIUM ON GEOLOGY
OF SE ASIA AND ADJACENT AREAS, HÀ NỘ I NOV. 1995


]. PHẠ M KIM NGÂN, LIJƠ N(Ỉ Hồ NG IIIỌ c • Cambrian and Ordovician sediments in Việ t Nam.
2. TỐ NG DIJY THANH, HOIJ HONGFF.I, TẠ HỒ PHI JONG, Ní ỉ IIYỄ N IlfJtJ HIJNG, ĐOÀN
NI1Ậ T TRIJONG. Outlines of stratigraphy and remarks on paleogeography of Devonian in
.Southeast Asia.
3. DIC'KINS J.M. Permian and Triassic events in Việ t Nam and implications for economic
geology.
4. NGUYÊN KINH Q u ố c , LÊ HIJN(Ỉ . Early Mesozoic feiTohypersthene - bearing volcano plutonic rocks from association group of klionlanite - dellenite - baclieitc in Northeast Việ t Nam.
5. NGÔ THỊ PHUỢ NG. Petrology and evolution of the formation of Permian - Triassic mafic ultramafic associations in North Viộ t Nam.
6. BROOKFIELD M.E. Reconstruction of Western Sibumasu.
7.LÊ DZUY BÁCH. Precambrian folded complexes of SH Asia.
8.IIANTORO W.S., LAFONT R., HIED A s., HANDAYANI L., SEBOWO E., HADIWISASTRA
S. Ilolocene to Recent vertical movement in Indonesia: study 011 emerged coral reef.
9. NGUYÊN ĐÌNH XIJYEN, TRAN THỊ MỸ THẠ NH. Estimation of recurrence period of laree
earthquakes in a given place following the long - term variation of seismic activity.

1

10
35
40
59
65
81
93
115

JOURNAL OF GEOLOGY, SERIES B, № 7-8/1996
10. TẠ HOÀ PHUƠ NG, BAIJDIJ - SIJIRE V., LÊ VẦ N GIANG. Scolecodonts from the Bail
Thiuig Fonnation (Lower Devonian) in Khao Lộ c - Quả n Bạ area, Hà Giang Province.

11. NGUYÊN HOÀN, NGUYÊN NGOC, NCỈ UYÊN HŨƯ c ử Main pe riods of paleogeographic
evolution of the coastal zone during Pliocene - Quaternary in Việ t Nam.
12. NGUYÊN ĐÌNH MỘ C, LÉON DEJONGHE. Les filons de quarts à stibine de cẩ in Phả ,
province de Quả ng Ninli, NE du Việ t Níun.
13. NGƠ VẢ N BIJtl, PHẠ M VÀN NGỌ C, HOÀNG HŨtJ QUÝ. Poss ibilities of applying modem
magneto - telluric method to geothermal potential assessment through defining the reservoir and
hot dry rock structure zone.
CONTENTS OF JOURNAL OF GEOLOGY, SFRIHS A, 1996

121
127
133

139
147


Proceedings of the IGCP Symposium
on Geology of SE Asia, H anoi, M /1995

Journal of GEOLOGY
Series B, No. 7-8/1996, p. 10

OUTLINES OF STRATIGRAPHY
AND REMARKS ON PALEOBIOGEOGRAPHY
OF DEVONIAN IN SOUTHEAST ASIA
T6ng-Dzuy Thanh*, Hou Hong-fei**, Tạ Hoà Phư ơ ng*
Nguyễ n Hữ u Hùng***, Đoàn Nhậ t Trư ở ng***
*. Việ t Nam National University, Hanoi. 90, Nguyễ n Trãi Road. Đố ng Đa, Hà Nộ i. Việ t Nam.
**. Institute of Geology. 26 Baiwanzhuang Road. Beijing. 100037. China.

***. Institute of Geology and Mineral Resources. Thanh Xuân. Đố ng Đa, Hà Nộ i. Việ t Nam.
Abstract.TVỉ e exposures o f Devonian rocks are widespread in Southeast Asia — in
South China (Guangxi, Yunnan Provinces), 'Việ t Nam, Laos, Thailand and Malaysia.
This paper is only a first attempt at correlating the Devonian stratigraphy in this
region. The Devonian stratigraphy and containing faunas will be examined in the
frame o f the following suitable terraries. Tile South China and North Việ t Nam terrane includes the territories ofGuangxi, East Yunnan (South China) and North Việ t
Nam up to the Northeast bank o f the Sông M ã fault. The Indochina terrane com­
prises the North o f Central Việ t Nam, Laos and East Thailand. The Shan - Thai terrane comprises Western Yunnan, Shan States o f Burma, mainland o f Thailand and
West Malaysia. The main stratigmphic units from Lower to Upper Devonian and
their fauna assemblages are presented and correlated in the paper.
In most cases o f South China, Northeast Việ t Nam areas a gap took place in
Siluriari-Devonian boundary sequences. The lowermost formation o f Lower Devo­
nian consists o f the rocks o f "Old Red Sandstone" facies -- Lianhuashan Formation
in South China, Sika Formation in Northeast Việ t Nam. A similar formation takes
place in the Mid-Central Việ t Nam —Tân Lâm Formation.
The continuous Siiurian-Devonian boundary can be expected in the Sông Cả
Sections (North o f Central Việ t Nam and Northeast Laos), in West Yunnan; North
arid Northwest Thailand - East Burma; in Peninsula Thailand and Malaysia. In most
cases o f these sections the Lower Devonian consists mainly o f shale, mudstone with
more or less mixture o f carbonate components containing pelagic fauna.
The Middle Devonian (sometimes from Emsian) in most cases consists o f fossiliferous carbonate facies. A short gap took place in the interval o f Middle Devo­
nian in Northeast Việ t Nam and South China.
The continuous Devonian - Carboniferous boundary can be observed in South
China (for example Nanbancun section in Guangxi), North Việ t Nam and in some
section o f Indochina terranes such as East Thailand, Central Việ t Nam. Meanwhile
a gap took place in West Yunnan, North Thailand and others.
The most special fauna is the one o f South China and North Việ t Nam terrane
in which Lower Devonian contains a great number o f endemics o f diverse benthic
groups. In spite o f that, the common taxonomic genera show the closeness o f Devo­
nian fauna o f the Southeast Asia region and the European ones. Some Australianlike fauna elements were also found in Southeastern Asia, but at present it is prema­

ture to conclude that a part o f this region was derived from Gondwana.

10


INTRODUCTION
The Devonian rocks are differently
studied in Southeast Asia. In South China
(Guangxi, Yunnan Provinces), Việ t Nam and
Laos they are widespread and attract a great
number of works of geologists. The exposures
of them in Thailand and Malaysia are also
studied and identified by geologists from dif­
ferent countries. In Cambodia there are only
the supposed Devonian rocks. According to
the existing data the Devonian of these re­
gions may be examined in the following suit­
able teư anes (Fig.l).
- South China and North Việ t Nam
terrane. Devonian rocks are widespread in
Guangxi, East Yunnan (China) and North
Việ t Nam. In the tectonic aspect these areas
are considered as the main parts of the South
China block. In this paper the Sông Mã fault
is taken as the southern lim it of it, instead of
the Red River (Sông Hồ ng) one in the con­
ceptions of the other authors (Fig.). Practi­
cally the Red River (Sông Hồ ng) fault plays a
very important role in geology of region in
Cenozoic, but there is not the differentiation

in the marine facies and the fauna of Devo­
nian in North Việ t Nam (up to the Sông Mã
suture). The role of the latter in Devonian is
distinguished as the clear lim it between the
North and the Central Việ t Nam.
- Indochina terrane. This terrane
spreads from the territories of the North part
of Central Việ t Nam toward to Laos and East
Thailand. Cambodia is also considered as a
part of this terrane.
- Shan-Thai terrane. The Devonian
exposures are observed in W est Yunnan
(China), Shan States of Burma, main land of
Thailand and its peninsular. The Devonian of
West Malaysia is also examined in the frame
of this terrane.
Remarks on paleobiogeography of the
region will also be presented, the available
data show the closeness of Devonian fauna of
Southeast Asia and the European ones.

STRATIGRAPHIC DATA
SOUTH CHINA AND NORTH VIỆ T NAM
TERRANE

North Việ t Nam (Table 1)
1. Lowermost Lower Devonian
In North Việ t Nam the Lowermost Der
vonian succession begins with Red Beds (Si
Ka Formation) in the Northeastern mountain

area and with marine deposits in the North­
western one (Iridistrophia praew nbraculum
Beds). In more general stratigraphic classifi­
cation of the Devonian in Việ t Nam, these
units are grouped together as the Si Ka Re­
gional Stage (Table 1).
The Si Ka Formation consists of purplish
red conglomerates, sandstones, shales and
marls in some sections, which overlie the
Cambrian or Ordovician unconformably.
Some plant remains have been determined as
Bytrotrephis aff. antiqua and fishes are refered to Yunnanolepiformes and Polybranchiaspis cf. gracilis (Tong-Dzuy Thanh & Jan­
vier 1987). This formation is correlated with
the Lianhuashan Formation and the Lower
part of the Cuifengshan Formation of South
China (Tong-Dzuy Thanh, 1980, Tong-Dzuy
Thanh et al. 1988). It should be compared
with the Old Red Sandstone of Western
Europe and may be assigned to Lochkovian
(Gedinian).
The Iridistrophia praeumbraculum Beds
are the lowermost marine strata of the Lower
Devonian in the Northwestern mountain area
of North Việ t Nam. They consist of black
shales in the Sông Mua Formation (thickness
over 1800m) in the lower basin of Sông Đà
River. The fossils are poor and have been
collected only in the middle level of this for­
mation: Corals — Parastriatopora cf.
rzonsnickajae, Brachiopods — Iridistrophia

praeumbraculum, M esodouvillina aff. subinterstrialis, Platyorthis cimex and Crinoids —
Schvschcatocrinus astericus. These Iridistrophia praeumbraculum Beds are considered as
the lowermost level of the Devonian in the
Northwestern mountain area and can be as­
signed to the Lochkovian. The Silu­
rian/Devonian boundary could be probably
present in the interval between the underlying
Bó Hiề ng Formation (Silurian) and the level
of Parastriatopora cf. rzonsnickaiae in these
examined Beds.


Figure 1. Devonian exposures'in Southeastern! Asian terranes
1 South China - North Việ t Nam terrane: 1 1 Guangxi, 12 East Yunnan, 1
J Northeast
of North Việ t Nam, 14 . Northwest of North Việ t Nam.
2. Indochina terrane: 2 1 . Central Việ t Nam (2 Ia , Cù Bai sections, 2 Ib ■
Rào Cả i sections,
2 lc Sông Cả sections). 2 2 . Central Laos. 2 J , 2 4 ■ West Laos - East Thailand, 2 Ị . Cambodia.
3. Shan - Thai terrane: 31, West Yunnan, 3 2 ■ Shan States, 3 3 ..Northwest Thailaruỉ ,
34 . Peninsula Thailand and Malaysia.
fossiliferous
undetermined Devonian

12

rare fossils


2. Bắ c Bun Regional Stage

The Bắ c Bun Regional Stage was estab­
lished on the basis of the coư elation of m a­
rine deposits yielding the Howittia wangi As­
semblage (Hysterolites wangi in the previous
works). This unit comprises the Bắ c Bun
Formation in the Northeastern mountain area,
the upper part of the Sông Mua and the m id­
dle part of the Nậ m Pi a Formation in the
Northwestern mountain area and other
equivalents (Table 1). They consist mainly of
black muddy shales with intercalation of fine­
grained sandstone and marls, limestone lenses
in some sections. The most characteristic
fossils are Brachiopods — Howittia wangi,
Howellella mercuri, Cymostrophia stephani,
Chonetes mansuyi, Protathyris sp., Bivalves - Mytilarca (Plectomytilus) oviformis, Corals
in the upper part — Favosites subnitellus,
Squameofavosites kolymensis, Thamnopora
incerta. Fish fossils have been collected from
Eastern area of North Việ t Nam, in the lower
part of this unit —Polybranchiaspis sp., Szeaspis sp., Yunnanolepis bacboensis, Y. deprati,
Chuchinolepis dongmoensis, Vanchienolepis
langsonensis, Youngolepis sp. (Tong-Dzuy &
Janvier 1990). Recently the fish fossils of
"South Chinese" types {Songdalepis pustolatus) are collected and described from this
stage in the downstream Sông Đà River,
probable in the higher level than in the East­
ern area (Janvier et al. 1996). The Bắ c Bun
Regional Stage yielding the Howittia wangi
fauna is probably Early Pragian in age.

3. Mia Lé Regional Stage.
By its abundant fossils this Regional
Stage is the most characteristic unit among
the Devonian strata in North Việ t Nam. It
comprises a combination embracing all for­
mations and beds characterized by the Euryspirifer tonkinensis fauna such as Mia Lé,
Bả n Nguồ n, Đạ i Thi Formations, Upper part
of Nậ m Pìa Formation, Lower part of Dư ỡ ng
Độ ng Formation and others (Table 1). Irs
stratigraphic sections consist of shales, fine­
grained sandstones and marls, sometimes
with limestone interbeds or lenses. In the
Northwestern mountain area the terrigenous
components increase in the sequences while
the carbonate components are more abundant

in the Northeastern mountain area. In the Hạ
Lang region and the northeastern coastal land
this unit consists only of terrigenous rocks.
The
characteristic
F.iiryspirifer
tonkinensis fauna is the most diverse Devo­
nian fauna assemblage in North Việ t Nam
and South China. Over 300 species of various
benthic groups have been determined and de­
scribed in North Việ t Nam, among them
Brachiopods and Corals are the most abun­
dant. Apart from numerous endemic species
many Mediterranean ones are found in the

association of this E uryspirifer tonkinensis
fauna, such as Corals — Favosites styriacus,
Squameofavosites cechicus, Thamnopora incerta, Roemeripora bohemicus, Heliolites
barrandei, H. praeporosus, Holmophyllum
holmi, Brachiopods — Acrospirifer primaevus, Leptaenopyxis bouei, H ow ellella m ercuri

etc.
On the whole, the generic taxa of the
tonkinensis fauna are as follows: Stromatoporoids — Anostylostroma, Atelodictyon,
Parallelostroma, Plectostroma, Praeidiostroma, Simplexodictyon, Stelodictyon, Stromatopora, Syringostromella, Vicinustachyodes, Trupestostroma; Tabulate — Fossopora,
Favosites, Emmonsia, Squameofavosites,
Riphaeolites,
Echyropora,
Cladopora,
Gracilopora,
Striatopora,
Thamnopora,
Parastriatoppora, Yacutipora, Roemerpora,
Alveolites, Crassialveolites,
Caliapora,
Coenites,
Tyrganolithes,
Syringopora,
Thecostegites,
Heliolites,
Paraheliolites,
Chaeteies, Chaetetipora; Rugoses — Tryplasma, Holmophyllum, Microplasma, Glossophyllum, Phollidophyllum, Cysticonophyllum, Cyathactis, Evenkiella, Pseudozonophyllum, Dialythophyllum, Zelolasma, Rhyzophyllum; Brachiopods —Acrospirifer, Aceptalium,
Athyris, Athyrisina, Atrypa, Desquamatia,
Aulacella, Chonetes, Cymostrophia, Dicoelostrophia,
Douvillina,

Euryspirifer,
Glossinotoechia, H ow ellella, Howittia, Indospirifer,
Leptaena,
Letaenopyxis,
Levenella, Megasirophia, M eristella, Parachonetes, Parastronella, Pletorhyncha, Pugnacina, Schellwienella, Stropheodonta, Thiemella, Uncinulus, Undispirifer etc. ; Bivalvia
Modiolopsis,
M ytilarca,
Pteria
(.Actinopteria), Pterinea (Pterinea), Pterinea
13


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Table 1. Devonian stratigraphie units in North Viêt Nam

ÜJ

Fauna

U


('Cornellites), Pterinea Ợ olmaià), Dissonia;

Nậ m Tát Regional Stage and consists of light
grey limestones. Only in the successions
along the coastal land and in some islands of
the Bắ c Bộ (Tonkin) gulf this level is charac­
terized by sandstone and shales of Dư ỡ ng
Độ ng Formation. Its abundant Coral and
Stromatoporoid assemblages correspond to
4. Bả n Páp Regional Superstage
the
Eifelian ones in other regions. The follow­
The dark grey stratified limestones of
ing
pelagic species are noteworthy — ViriEmsian-Givetian age are largely observed in
atellina
dalejensis, V. irregularis, V. aff.
North Việ t Nam (Table 1) and have been de­
richteri,
Nowakia
cancellata.
scribed under various names such as Bả n Páp,
- T h e upper level corresponds to the Hạ
Nà Quả n, Hạ Lang, Bằ ng Ca, Mó Tơm, Lỗ
Lang Regional Stage and consists mainly of
Sơ n, Tràng Kênh stratgraphic names in previ­

dark grey limestone with intercalation of
ous publications. They consist of various
cherts in several sections, in particular in the
kinds of limestones and Tong-Dzuy Thanh
sections near Việ t Nam - China border. Cor­
(1993) has combined them into the Bả n Páp
als and Brachiopods are predominant and the
Regional Superstage. On the whole the for­
components of the Caliapora battersbyimation components of this superstage are
Stringocephalus burtini Assemblage are char­
distinguished in three levels.
The lower level corresponds to the Pắ acteristic
c
fauna of the Hạ Lang Stage. Some
characteristic species are as follows — AmNậ m Regional Stage. Its component forma­
tions compose mainly of well-stratified bi­
phipora ramosa, Actinostroma clathratum,
tuminous, muddy limestones overlying con­
Thamnopora nicholsoni, Caliapora battersformably the Mia Lé Stage. In several sec­
byi, Scoliopora denticulata, Grypophyllum
tions, especially in the northern land near the
isactis, Dendrostella trigeme, StringocephaViệ t Nam-China frontier, intercalation of thin
lus burtini (Tong-Dzuy Thanh 1993). Pelagic
beds of cherts is present. Generally, Corals,
fauna are inadequate studied, few species
Stromatoporoids and Brachiopods are abun­
were identified — Nowakia aff. otomari, Virdant in almost sections of this stage. But
iatellina multicostatus, Polygnathus xylus
Dacryoconarids and Conodonts are important
xylus, Panderodus sp., Spathognathodus sp.

fossils in the sequences with the intercalation
It is worth noting that in the Lạ ng Sơ n
of cherts. In its lowermost beds overlying
Province, near Việ t Nam - China border (Sông
conformably the Mia Lé Formation of the
Hiế m) section in the Middle level of the Bả n
Đồ ng Văn - Sông Nho Quế section (Fig. 2),
Páp Superstage a terrigenous clastic formation
Dacryoconarids of zlichovensis zone and rep­
bearing Lepidodendropsis Flora takes place in
resentatives of Nowakia acuaria, Conodonts
the sequences (Table 1). This event was
of perbonus zone have been identified (Ta
probably caused by a local movement during
Hoa Phuong 1994, Tong-Dzuy Thanh & Ta
the Middle Devonian in the Northeast of
Hoa Phuong,
1994). Recently Tạ Hoà
North Việ t Nam. On basis of the containing
Phuong record the following Conodonts and
fauna, one of us has identified the Bả n Páp
Daeryconarids in the lower part of the Đồ ng
Superstage as Emsian-Givetian in age (TongVăn - Sông Nho Quế section of the Pắ c Nậ m
Dzuy Thanh 1988, 1993). Correspondingly
Stage from the bottom upward: 1) Nowakia
the Pắ c Nậ m Stage is Emsian, the Nậ m Tát
acuaria, 2) N. zlichovensis, 3) N. mana,
Stage — Eifelian and the Hạ Lang one —
Polygnathus nothoperbonus, Pol. gronbergi.
Givetian in age.

- T h e Middle level corresponds to the

Trilobites — Gracicalymene, Phacops, Proetư s, Plagiolaria, Ductina, Otarion; Crinoids - Hexacrinites; Dacryoconarids — Styliolina,
M egastyl iol ina.

15


Table 2
STA6E

AGE

ZONES

c,
T

0

T

A

T

CONODONT

sulcata

FORAMINIFERA
ZONES

Chemyshinella

praesulcata) â Quasiendothyra1
(expansa)
đđđ
FApostera
Uralinella - Septađ
glomospiranella
trachytera
â
MEN- marginifera
â (D đ
rhomboidea
(D
NIAN crepida ®
»a. triangularis
® (D ®
gigas ® ®
Tikhinella multi­
formis - Eonodosaria
FRASevlanensis
К . triangularis
©
NIAN (Pol. assymmetricus)

Table 2. Conodont and Foraminifer zones in
the Tố c Tát Stage (Upper Devonian).

Number in circle after ử ie zone name show the
distribution in : © - Tố c Tát section, @ - Đồ ng
Vãn - Sông Nho Quế section, ® Bả n cả i section
(Sơng Đà in Northwest Bắ c Bộ ). Zone name in
parentheses: the index species of die zone has not
been found yet.
5. Tố c Tát Regional Stage
This regional stage has been established
by incorporating all the forcnations of Upper
Devonian such as Tố c Tát, Bả n Cả i Forma­
tions (Table 1) and their equivalents in differ­
ent areas, which conformably overlie the Hạ
Lang Stage in Bắ c Bộ (North Việ t Nam) re­
gion. Excluding a part of the Upper Devonian
in the Northeastern coastal land, the Tố c Tát
Stage comprises striped cherts, siliceous
1 In the top of the Tố c Tát section some first rep­
resentatives of Chemyshinella zone have been
also found.
16

shales in intercalation with marls and finestratified limestones. The intercalation of
variegated, nodular limestones is observed in
the Hạ Lang and Đồ ng Văn - Sông Nho Quế
sections near Việ t Nam - China frontier. In
the Tố c Tát section of Northern area and in
the lower basin of Sông Đà (Northwestern
area) the conformability is observed between
the top of Tố c Tát Stage and the Lower Car­
boniferous limestone. Several samples of

Brachiopods, Bivalves have been found, but
important role belongs to Conodonts and Foraminifers. Distributions of the latter from
bottom upward in Tố c Tát, Đổ ng Văn - Sông
Nho Quế and Bả n Cả i (Sông Đà in Northwest
Bắ c Bộ ) sections are shown in the Table 2.

South China
Devonian deposits are widespread in
Guangxi and East Yunnan Provinces
(Devonian in West Yunnan will be presented
in the frame of Shan - Thai terrane). Their
stratigraphic sequences are well known, es­
pecially in Guangxi where typical sections
have been well studied. Marine deposits of
Devonian in South China have been described
in different units which are distinguished into
two facies types namely Xiangzhou type and
the Nandan one.
LOWER DEVONIAN

Lianhuashanian Stage
The Lianhuashanian chiefly consists of
purplish red siltstone, mudstone, with argil­
laceous limestone in the middle part, thickbedded quartzose sandstone at the base. The
important fossils are Vertebrates — Galeaspis
sp., Asiaspis expansa, Asiacanthus suni, A.
kaoi, Yunnanolepis sp.( Lianhuashanolepis
liukingetisis, Orientolepis neokwangsiensis.
The typical section of the Lianhuashan
Formation has been described in Liujing area

(Guangxi), here entire sequence of the forma­
tion reaches to 360m in thickness. The red beds of Lower Devonian in other areas of
South China are differently correlated. In
Nandan and Xiangzhou (Guangxi) they are
corresponding to all Lianhuashanian and
Nakaolingian and reach to more or less
1000m thickness. At the mean time the red -


beds in East correspond to all the sequences
from Upper part of Lianhuashan to the top of
Nakaoling Formation. Just in those red-beds
abundant fish as.semblage have been collected
and studied, among them the well-known are
the diverse species of genera: Polybranchiaspis, Eugaleflspis, Yunnanolepis, Chuchinolepis, Galeaspis, Yunnanogalaspis, Youngolepis, Szelepis, Orientolepis, Asiacanthus etc.
Numerous Vertebrates bave been recorded
from the Chifengshan Formation o f Eastern
Yunnan. Some of them generic taxa can be
referenced from Pan and Dineley (1988):
Hunanaspis, Eugaleaspis,
Yunnanolepis,
Quijinolepis, Napanaspis, Polybrachiaspis,
Szelepis, Phymolepis, Youngolepis, Diabolepis,
Yunnanogaleaspis,
Dongfangaspis,
Kwangnanaspis, Asiacanthus.
Nakaolingian Stage
The components of this stage are greyish-green calcareous mudstone intercalated
with thin-bedded or lenticular limestone. Im­
portant fossils are follows: Brachiopods —

Orientospirifer nakaolingensis, O. wangi2 ,
Aseptalium guangxiensis, Kwangsirhynchus
liujingensis,
Corvinopugnax
globosus,
Prothathyris praecursor, Chonetes ellipticus.
Corals — Chalicidophyllum nakaolingensis,
Eoglossophyllum minor. Conodonts — Eognathodus linearis postolinatus, Hindeodella
equidentata, H. priscilla, Trichonodella excavata, Eognathodus sulcatus, Pandorinellina exigna exigna, Panderodus striatus
striatus etc.
Only in the Luijing area (Guangxi) the
Nakaolingian Stage is characterized by marine
facies, in other areas it corresponds to the red
- beds of the Lower Devonian.

Brachiopods — Diverse components of
the
Dicoelostrophia
Rostrospirifer
tonkinensis3 Assemblage, Nadiastrophia
yukiangensis, Pdrachonetes nasatus, Parathyrisina tangnae, Howellella papaoensis,
Acrospirifer ordinaris, Elimospirifer kwangsiensis. Corals: Xystriphylloides nobilis, Heterophaulactis semicrassa, Xyhonophrentis
angusta, Amplexiphyllum hamiltoniae etc.
Trilobites — Gravicalymene maloungcaensis,
Proetus indosinenis, Dechenella luijingensis.
Conodonts —Polygnathus dehiscens, Neoprioniodus bicurvatus, Spathognathodus exiguus
guangxiensis, S. optimus, Ozarkodina denckmani, Hindeodella priscilla etc.
All the formation components of this
stage embody the platform marine facies with
abundant benthic fossils of Dicoelostrophia Rostrospirifer

tonkinensis
assemblage
(Yukiang and Yilan Formations in Guangxi,
Pojiao Formation in East Yunnan).
MIDDLE DEVONIAN

Yukiangian Stage
The most abundant fossil unit consists of
mudstone, calcareous siltstone, argillaceous
limestone intercalated with biogenetic lim e­
stone. Fauna are very abjindant and diverse in
taxonomic components, some of them are
noted as follows:

- The Xiangzhou type is composed of
bioclastic limestone, dolomite and marl
commonly intercalated with terrigenous clas­
sics. The rocks are widely spead in Northern
area of Guangxi province and Southern area
of Guizhou province. The biota consists
mainly of benthos, especially Corals and
Brachiopods. The most characteristic fossils
of Eifelian are the presentatives of
Xenospirifer fongi Assemblage Zone and
Acrospirifer houershanensis
Utaratuia
sinensis Assemblage Zone. The Well-known
Givetian Brachiopod of Stringocephaus
burtini and Tentaculites o f Nowakia otomari
are indicated species for the Tungkanglingian

Stage.
- The Nandan facies type is composed
mostly of biogenic limestone, dolomite, sili­
ceous rock and black carbonaceous rocks.
The rocks widely occur in East Yunnan and
South Guangxi. The biota is characterized by
pelagic fauna of cosmopolitan character such
as Tentaculites, Ammonoids. Among pelagic

2 In Việ t Nam this species is named as Howittia
wangi or Hysterolites wangi

3 Euryspirifer tonkinensis in the works of Viet­
namese authors

17


fauna the common Eifelian species are
Nowakia cancellata, N. richteri, N. sulcata,
Anacestes noeggerati, Pinnacites jugleri.
UPPER DEVONIAN

Diverse units o f Upper Devonian in
South China have been described and they are
assigned in two stages — the Shetienchiaoian
and the Hshikuangshanian. In the Xiangzhou
facies type they consist mainly o f different
kind of limestone bearing benthic fossils but
they are well identified by Conodonts. In the

Nandan facies type (Eastern areas of Yunnan,
Southern areas of Guangxi) they are com­
posed of mudstone, siliceous limestone and
nodular limestone. The pelagic fossils are
common in these units such as Conodonts,
Ammonoids although some Brachiopods are
collected. Thanks to the studied Conodont
assemblage this pair units of Shetienchiaoian
and the Hshikuangshanian formations are cor­
respondingly correlated with the Frasnian and
the Famennian.
On the age o f the tonkinensis fau n a in
South China and North Việ t Nam
The Euryspirifer tonkinensis fauna
(= Rostrospirifer tohkinensis fauna in many
works of Chinese geologists) is widespread in
both South China and North Việ t Nam (up to
the Sông M ã suture). The index species of
this fauna was first described by Mansuy
(1908), other geologists from "Service
Géologique de l'Indochine" considered it as
Spirifer speciosus (Saurin 1956). Represen­
tatives of the endemic genus Dicoelostrophia
are also wide-spread in both South China and
North Việ t Nam. So this fauna has been
named
as
Euryspirifer
tonkinensisDicoelostrophia fauna by Hou and Xian
(1975). It is worthy to note that in Việ t Nam

representatives of the Dicoelostrophia genus
are usually not found from the high level of
the strata bearing Euryspirifer tonkinensis
fauna.
It is relevant to draw attention to the pe­
culiarity of this assemblage in North Việ t
Nam, various older forms were found to­
18

gether with the Lower Devonian species.
They are, for example Holmopkyllum holmi,
Howellella mercuri and others. The pelagic
faunas of the M ia Lé unit are still feebly
studied in Việ t Nam, but Conodonts of the
nothoperbonus zone and Dacryoconarids of
the acuaria and zlichovensis zones have been
found from the lowermost, level of the overly­
ing beds (Ta Hoa Phuong 1994, 1996).
For a long times the age of the Euryspirifer tonkinensis fauna was a controver­
sial subject in geology of the region (TongDzuy Thanh, Ta Hoa Phuong 1994, Hou H.
F. 1996). Mansuy (1908), Deprat (1915) as­
signed it to Gothlandian, but it was assigned
an Eifeiian age by Jacob and Bourret (1920),
Saurin (1956), Dư ơ ng Xuân Hả o et al. {in
Dovjikov et al. 1965), Dư ơ ng Xuân Hả o et al.
(1980). Recently in Ỷ ìệ t Nam this fauna has
been considered as Pragian in age, while Chi­
nese geologists identified it as Early Em sian;
some time — Late Pragian - Early Emsian in
age. Hou H. F. (1996) gives a minute history

of the debate on this question and presents the
distribution of the Euryspirifer tonkinensis
fauna in Devonian sequences of both South
China and North Việ t Nam. After all he
brings forward a new views that "the top of
the strata bearing tonkinensis fauna is
diachronous". This viewpoint seems to be
reasonable, when the facies changes the con­
taining fauna must change too. That's why in
the pelagic facies bearing Emsian Conodonts,
Dacryoconarids of North Việ t Nam the Euryspirifer tonkinensis fauna are not found and
the bearing strata of the latter are considered
older than the ones in South China. This in­
terpretation does not conform to the data from
Devonian sections in North Việ t Nam. A
great number of Emsian benthic fossils have
been found in the overlying Pắ c Nậ m Stage,
but there is no trace of Euryspirifer
tonkinensis in here. Furthermore, in the M á
Lủ - Đồ ng Văn section (Fig. 2) in the first
beds of the Bả n Páp Formation (~ Nà Quả n
Fm.), that cover the M ia Lé Formation, Ta
Hoa Phuong has newly reported the following
fauna of in ascending order:
1)
Nowakia acuaria 2) N ow akia zlichovensis, 3)
N. mana, Conodonts of excavatus and nothoperbonus zones, Nowakia barrandei, etc.
(Fig.2).

I
f T

I

X

II

5/.

r

cooperi. Si. crenulata
Hindeodella subtiHs
P. com m unis
Ha. m a r g im t e r a

R
I =' FI Ĩ ' I
: I : I—
-H r-i
H -H -t
-H -t
t ±±±
I
-t-H + -H H -j-H

Pa. glabra acut a
Pa. m in u t a , Pa. glabra

i-H - t- H -

i-T -H I

-t-H -

Pa. subrecta. An. nodosa
Pa. triangularis
Pa. gigas
Pa. proversa, H. krest ovnikovi

-H -tz
<

a
•

z

o
>

‘ ~ì 1 T

ID

D

m

s
.
,

P. varcus, N. otom ari
P. serotinus, P. Unguiformis
Nowakia richt eri
N. cancel lata
N. elegans
Viriatellina huyeni sp. n.
N. barrandei,
N. mana, Pol. nothoperponus.
Pot. gonbergi,
N. zlichovensis
N. acuaria

Bent hic fossi/ s o f
Euryspirifer tonkinensis Fauna

Figure 2. Devonian fauna levels in the Má Lũ - Đồ ng Văn s ection (Đồ ng Văn - Sông Nho
Quế region, Hà Giang Province, North Việ t Nam).
Mia Lé Formation - Members 1-2: Intercalation of shale, mudstone, limestone with
abundant benthic fossils o f Euryspirifer tonkinetisis assemblage.
Bả n Páp Formation (former N à Quả n Fill.)
-- Member 3: Intercalation of black grey
limestone, siliceous marl, chert. Member 4: Grey light limestone with interbeds o f siliceouslimestone.
Tố c Tát Formation: Striped, variegated limestone with intercalation of thin bedded cherts.
Đa Niêng Formation: Intercalation of dark grey limestone, siliceous limestone containing
Lower Carboniferous fauna.

19


Other questions can be put on this subject —
do the Brachiopod fossils in the top of the
strata bearing tonkinensis fauna o f South
China belong to the genuine Euryspirifer
tonkinensis fauna? Are there the same repre­
sentatives
of the
Mansuy's
"Spirifer
tonkinensis" in here? In any case, with the
present materials the age o f the tonkinensis
fauna and in relation of that the age o f its
bearing strata in South China (Yukiang) and
North Việ t Nam (Mia Lé) should be consid­
ered as an open question.
INDOCHINA TERRANE
Devonian exposures of this teư ane are
observed from the North part of Central Việ t
Nam toward Laos and East Thailand. Devo­
nian facies of the Eastern territory of Laos is
very close to the one of Central Việ t Nani and
up to the Southern border of Sông M ã fault. In
the meantime the facies of scarcely Devonian
exposure in West Laos is similar to the one of
East Thailand. Cambodia is a part of this terrane but up to now there has been no evidence
for identification of the Devonian in this terri­

tory.
CENTRAL
GION (Table 3)

VIET NAM - LAOS RE­

From the Mid-Central .Việ t Nam north­
wards to the Sông M ã suture Devonian facies
are distinguished into three section types
namely Cù Bai, Rào Cả i and Sông Cả , the
same facies of each type are observed in the
East of Middle and Northern Laos. The
northern border of this distribution area is
edging along the south side of Sông M ã fault
upwards to the North of Việ t Nam - Laos
frontier. The facies of the lowermost Devo­
nian is changed from the South to the North,
in the South that is nearly neighboring with
the Kontum block structure it characterizes by
Red Beds sandstone and northward by marine
facies. From Givetian the platform facies is
widespread in all sections of this area.

20

Lower Devonian
- In the Sông Cả area, that is at southern
side of the Sông M ã suture northwards along
the Viộ t Nam-Laos frontier to the Northwest
of Việ t Nam (Fig. 1), the lower Devonian is

considered as a part of the Huổ i Nhi Com­
plex. The latter consists of thick flyshoid suc­
cession of shales, fine grained sandstones ob­
served from the West o f Nghệ An Province
northwards along thé ỴWO sides of the Việ t
Nam - Laos frontier to the W est of Điệ n Biên
Phủ townlet. Pelagic faunas have been re­
corded: Nowakia cf. acuaria, Styliolina sp.,
Erbenoceras cf. advolens, Anetoceras sp. .
Plant remains of Zosterophyllum sp., Rhynia
spj, Protopteridium sp. have been found in
the lower part of this complex. In the higher
level Nowkia zlichovensis , N. barrandei
have been recorded. It is relevant to note that
in some sections considered as belonging to
this Huổ i Nhi Complex some Middle Devo­
nian fossils have been collected such as
Nowakia holynensis, Viriatellina cf. holardi,
Distriatostylus cf. akkaensis, Styliolina cf.
nucleata, Homoctenus sp. ect. Due to the
complicated geologic structure o f the region
this unit is considered as a stratigraphie
complex. In expecting the clarity of the real
succession of this unit, its main substance is
temporarily assigned to Lower Devonian.
A similar succession is well observed in
Xieng Khouang and Hua Phan (Samneua)
Provinces of Laos. In the mapping works in
these areas Vietnamese geologists collected
near village Ban Ban Nowakia cf. zlichovensis, N. barrandei.

- In the territory of Hà Tĩn h and North of
Quả ng Bình Provinces (Rào Cả i section type)
the Lower Devonian consists mainly of
shales, sandstones named Rào Chan Forma­
tion that unconformably overlies the Đạ i
Giang Formation. The rocks of this formation
extend their distribution in adjacent area of
Mid-Laos. A few fossils have been found
such as Brachiopods Desquamatia vijaica,
Crinoids Lissocrinites curtus, Hexacrinites
(?) hwnilicarinatus.


- In the South of this region (CÙ Bai sec­
tion type) the Lowermost Devonian consists
of conglomerates, of fine-grained Red sand­
stones of Tân Lâm Formation unconformably
overlying the Upper Silurian Đạ i Giang For­
mation. The red colour of the rocks, variable
thickness and other properties of the forma­
tion reminiscent of continental facies of the Si
Ka Formation in North Việ t Nam. Some Lingula have been found and identified such as
Lingula cornea Sow., L. aff. hawkei Rouault,
etc.

In any case, the above data are rather scat­
tered ones that have been achieved in the pre­
liminary study on a large area of Laos and
Thailand. No new systematic studies on De­
vonian have been made in these areas, so it is

difficult to define exactly the real sequences
and to correlate them with the ones of the
adjacent areas. The only one thing that must
be clearly noted is that though with its poor
components this Devonian fauna is very close
to the one of Việ t Nam and of Eurropean re­
gions in common.

- In Mid-Laos.
A succession of sandstone and shale with
limestone interbeds exposes in Kam Keut,
Nam Tchong and Tham Ta On villages of
Tran Ninh plateau (Laos). Brachiopods -and
Corals have been recorded by Saurin (1955)
and Fontaine (1954): Indopirifer padaukpinensis, Atrypa reticulata, A. aspera, Chonetes
nongpoensis, Schizospirifer multiplicatus,
Orthotetes umbraculum, Favosites goldfussi,
Fav styriacus, Fav. eifeliensis.
- In East Thailand and W est Laos. De­
vonian marine deposits are outcropped in
Loei district, in Ban Muang and Ban Chom
Noi westward from Vientiane. In Thailand
they are considered as an upper part of the
Pak Chora Formation, the latter consist
mainly of shale, limestone with intercalation
of chert, but limestone is widely spread in
Loei region. The similar succession of grey
limestone is outcropped around Pak Lay and
Ban Vang (Xaynha Buri Province of West
Laos) near Vientiane. From here Fontaine

(1954, 1990) has reported Corals —Favosites
styriacus, Fav. goldfussi, Fav. cf. ottiliae,
Heliolites porosus, etc.
Saurin (1956) and Fontaine (1954) have
assigned these successions to Eifelian, but in
correlation the mentioned fauna with the ones
of Việ t Nam they m ust be older and at least
should be Emsian. Recently from these lo­
calities Fontaine et al. (1990) noted the pres­
ence of Favosites styriacus, Fav. goldfussi,
Fav. cf. ottiliae, Fav. aff. nitidus, Emmonsia
sp., Squameofavosites sp., Heliolites porosus,
Algae of genus Renalsis. The latter authors
conclude that the limestone yielding these
fossils is Early Devonian and ?Eifelian in age.

M iddle Devonian
From Middle Devonian the platform car­
bonate facies are step by step developed in the
Devonian sequences of the Central Việ t Nam
- East Laos region.
- In the Sông Ca area, the H uổ i Lôi
Form ation (about 650m thickness) consists
mainly of black - grey sandstone, shale in
intercalation with thin beds of marl and
limestone. Calceola (?) sandalina and Hexacrinites humilicarinatus and Brachiopods of
Howellella
sp.,
Stropheodonta
sp.,

Acrospirifer sp. were collected in sandstone
of the lower part (about 300m thickness)
while in the thin limestone and marl interbeds
of the middle part Corals are rather abundant - Favosites goldfiissi, Thamnopora cf. savis,
Th. kolodaensis, Trachypora dubatolovi,
Coenites quydatensis, Egosiella cf. safonoviensis, Trypanopora sp., Chaetetes yunnanensis, Utaratuia cf. pinhuangshanensis and
Stromatoporoids Stachyodes insignis. The up­
per part (150m of sandstone and shale) con­
tains Dacryoconarids Homoctenus sp., Styliolina sp.
Judging the collected fossil, the middle
and upper parts of the Huổ i Lôi Formation
should be Middle Devonian in age while the
fossils of its lower part still express the late
Earlv Devonian appearance.
- In the Rào Cả i area (section type) the
Middle Devonian comprises three formations
namely Bả n Giàng, Mụ c Bãi and Độ ng Thờ
ones. The Bả n Giàng Formation reaches to
850 -1000m thickness and consists of diverse
kinds of sandstone with mudstone and shale
interbeds, limestone lenses in the lower part.
Two levels of fauna have been reported, the

21


first in the lower part of the formation which
comprises a poor association of Calceola
sandalina, Stropheodonta sp., Howellella sp.,
Desquamatia aff. lanceoides, Hexacrinites (?)

humilicarinatus; and the second which has
noted in a limestone lense of the Khe Lớ p
section and contains Favosites multiformis,
Fav. cf. krekovemis, Parastriatopora aff.
dobretzovi, Heliolites porosus, Paraheliolites
cf. hanusi, Spongophyllum. halisitoides,
Thamnophyllum khelopense, Spongophyllum
sp., Pseudogrỵ pophyllum sp., Stachyodes sp.,
Stromatopora hupchii.
The majority of the above-mentioned
fauna shows that the Bả n Giàng Formation is
eifelian in age. It is relevant to note that the
fauna of the first level seems to be still close
to the Emsian while in the second fauna level
contains even some Givetian representatives.
It is difficult to define exactly the age of this
formation now, due to the lack of the data of
the study on Conodont and Dacryoconarid.
The M ụ c Bãi and Độ ng T hờ Formations
are considered as a pair of the nearly syn­
chronic units (Table 3). The M ụ c Bãi For­
mation consists of sandstone in intercalation
of limestone, muddy limestone that reach to
450m thickness. The peculiarities of this for­
mation are the unstable thickness of its com­
ponents and the abundance of its benthic
fauna. A great number of different benthic
groups such as Stromatoporoids, Tabulates,
Rugoses, Brachiopods, Crinoids, Bryozoạ
have been identified from this formation. In

upward order they can be divided into three
Givetian assemblage zones namely Undispirifer undiferus - Chonetipustula orientalis,
Stringocephalus burtini - Caliapora battersbyi and Emanuella ronensis - Schizophoria
ivanovi. The Độ ng T hờ Formation consists
mainly of sandstone, mudstone and shale of
unstable thickness from some ten meters to
500 - 600m, thin marl beds are also observed
in the lower level of the formation. Me­
gafossils are sparse in the succession of ihe
formation, some Brachiopods like the ones of
the Mụ c Bãi Formation were reported such as
Undispirifer cf. undiferus, Emanuella sp.,
Schizophoria ivanovi, Spinulicosta spinulicosta, Atrypa reticularis etc. (Tố ng Duy
Thanh, Vũ Khúc, 1995). Plant remains of

22

Lepidodendropsis sp. and abundant spore as­
semblage show that this formation is Givetian
in age like the Haikou Formation in South
China (Tong-Dzuy Thanh, Cai Chong-yang
1995). Described fish remains offer important
evidence in the paleogeographic comprehen­
sion of the region. [Tong-Dzuy Thanh, Jan­
vier Ph., Doan Nhat Truong 1994 (1995),
Tong-Dzuy Thanh, Ta Hoa Phuong & Janvier
Ph. 1996].
- In the adjacent area of Laos, that is in
the succession of limestone in Kam Keut
(Middle Laos) and in the one of shale in Nam

Tia (Tran Ninh Plateau) Givetian fossils were
reported such as Stringocephalus burtini in
the first and Ambocoelia haugi (=Emanuella
haugi), Leptaena rhomboidalis kwangxiensis,
Leptodesma jacobi in the second succession
of shale (Saurin 1956).
Middle and Upper Devonian
- In the Sông Cả area a succession of
dark-grey bedded limesone, with some shale
and mudstone interbeds, was described
piecement under the different stratigraphic
names such as Nậ m cắ n , Cát Đằ ng Forma­
tions, Huổ i Căng, Noọ ng Dị a Members, etc.
New study by Nguyễ n Hữ u Hùng shows that
these units are, in fact, the components of a
continuous succession, so he suggests to'
unify all of them in the Kỳ Sơ n Formation
(Tố ng Duv Thanh, Vũ Khúc, 1995). The total
thickness of the formation reaches to 550 600m. which can be divided into three parts.
The first one consists of grey limestone of
300m thickness yielding Givetian Stromatoporoids and Corals: Actinostroma expan­
sum, Stachyodes radiata, Amphipora ramosa,
Scoliopora denticulata, Thamnopora polyforata, Thamnophyllum sp, etc. In the second
part some shale interbeds are observed in the
succession of limestone (290m thickness)
yielding Stromatopora: Stachyodes costulata,
S. lagowiensis, A m phipora franca, Brachiopods: Desquamatia sp., Dacryoconarids: Homoctenus sp. and Frasnian Conodonts — Palmatolepis gigas, p . foliacea, Ancyrognathus
triangularis. The uppermost part consists of
shale and light grey striped limestone of
170m thickness bearing Famennian Conodonts: Palmatolepis glabra glabra, p . perlobata schindewolfi, p. trachytera.

Table 3. Devonian stratigraphie units of Indochina terrane


Gracilopora polonica, Alaiophyllum incomp- In the Rào Cả i area (Hà Tĩiih and Quả ng
tum, Brachiopods: Cyrtospirifer sublimis,
Bình Provinces) Upper Devonian comprises a
succession (about 200m thickness) of thick
Cyrtosp. echinosus, Cyrtosp. postarchiaci,
bedded, light grev limestone and striped
Cyrtiopsis graciosa, Uchtospirifer nalivkini,
limestone in the upper part. They have been
Uchtosp. concentricus, Uchtosp. tanlarnensis.
described as Xóm Nha Formation (Cát Đằ ng
The second association of this upper level
Formation by others). BiostratigrahicaUy this
contains Famennian fossils such as Foformation can be divided into two levels, the
raminifera -- Quasiendothyra kobeitusana, Q.
first coư esponds to the lower member (70m
communis, Stromatoporoids — Stromatocethickess) and the second one (100m thickess).
rium kwangsiensis, Labechia obscura, PseuThe first member consists of light grey
dolabechia aff. huanjiangensis, Corals — Sylimestone yielding Frasnian Stomatoporoids,
ringopora geniculata haiphongensis, s. re­
Corals such as Stachyodes costulata, s. anguticulata, S. distans, Cystophrentis kolaolata, S. parallelopora, s. lagowiensis, Thamhoensis, Zaphrentoides sp., Brachiopods -nopora polyforata, Scoliopora aff. denticuYunnanellina hanburyi, Y. aff. triplicata. The
lata, Temnophyỉ lurn iseiense, T. cf. lantenoisi
mentioned fauna assemblages show that the
and Conodonts of Palmatolepis gigas. The
CÙ Bai formation should be Late Givetian second member comprises dark grey muddy
Famennian in age. It is relevant to note that in

limestone containing Conodonts from Pa.
the bottom of some section, for example in
rhenana to Pa. linguiformis zones. The sec­
the Tân Lâm Quarry some fossils seem to be
ond level corresponds to the middle and the
older while the top of the formation contains
upper members containing- numerous Faforaminifera of Toumaisian appearance. Due
mennian Conodonts from the Pa. triangularis
to the lack of the Conodont data, it is difficult
zone to the Pa. marginifera one.
to solve this problem now.
In the CÙ Bai area a formation of the
New data on Givetian - Frasnian have
same name consisting of dark grey bedded
been recorded from the limestone succession
limestone, muddy limestone with siliceous
around Vientiane and in Xieng Khouang
limestone interbeds in its middle part. Biosprovince. The latter succession may be in the
tratigraphically it can be divided into two
level higher than the one of the above men­
levels, the first corresponds to Givetian tioned Emsian limestone. Nguyễ n Hữ u Hùng
Lower Frasnian, the second is assigned to
determined Amphipora ramosa, A. rudis, A.
Upper Devonian. In the first level following
rara, A. laxeperforata, Idiostroma fililam ifossils have been reported — Stromatoporoids:
natum.
Amphipora ramosa minor, A. rudis, A. pinFontaine et al. (1990) described a suc­
guis, Corals: Crassialveolites cf. crassus,
cession of limestone in Ban Muang, Ban
Scoliopora aff. denticulata, Argutastrea

Khok Phai, Ban Chom Noi, Phu Thanon of
lavali, Disphyllum sp., Grypophyllum sp.,
Northeast Thailand, Westward from Vienti­
Brachiopods: Emanuella ronensis, Schizoane. Numerous Givetian - Frasnian fossils
phoria bistriata, Mucrospirifer novosibiriciis
have been recorded, such as Stromatoporoids:
vietnamicus, Athyris concentricus, Gypidula
Amphipora ramosa, A. angusta, A. rudis,
planispina, etc. Fossils from the second
Actinostroma cf. devoniense, Clathrodictyon
(upper) level can be examined in two associa­
sp., Stachyodes cf. insignis, Hermatostroma
tions, the first contains Frasnian species of
beuthi, H. cf. pustulotum, Corals: ThamForaminifera: Eogeinitzina devonica, Eononopora polygonalis, Th. cf. nicholsoni,
dosaria rara, Nanicella porrecta, TourGracilopora sp., Trachypora sp., Alveolites
nayella pussila, T. jubra, Tikhinella fringa,
cf. taenioformis, Al. ex gr. smithi, Al. cf.
T. multiformis, Stromatoporoids: Stachyodes
adm irabilis, Crassialveolites crassus, Cr. aff.
costulata, s. angulata, s. crebrwn, Amcrassiformis, Caliapora battersbyi, Coenites
phipora laxeperforata, A. pervesiculata,
ex gr. fascicularis, Heliolites p o r o su s , ChaeTienodictyon tschussovense, Atelodictyon
tetes yunnanensis, Ch. inflatus, Sinospongotrauscholdi, Corals: Alveolitella densata,
24


phyllum planotabulatum, Phillipsastraea
hennahi, Endophyllum abditum, Thamnophyllum cf. stachei, Dendrostelỉ a sp.

SHAN - THAI TERRANE

W ESTERN YUNNAN (Table 4)
The Devonian in Western Yunnan region
(west to Yuanjiang River = Red River = Sông
Hổ ng), is quite different from those of South
China. According to the facies and containing
fauna it could be examined in three zones
namely the Yuanjiang in the East, the Baoshan-Shidan in the mid-West and the Tengchong in the West. In the latter zone (West to
Nujiang River) Devonian rocks are scarce and
poorly exposed. The vast Lancan River
(Mekong River) reaches between Nujiang and
Yuanjiang Rivers are covered by MesoCenozoic deposits with Devonian unknown
(H ouH . F. 1994).
In the East o f this region the Devonian
deposits occur in the Lijiang area in the North
and in the Jinping- Mojang one in the South
along the West side of the Red River (Sông
Hồ ng) strike-slip fault (Fig. 1).
Lower Devonian consists mainly of
clastics and carbonates which can reach to
nearly 1000m thickness (Dazhongzhan For­
mation in the South and Alengchu, Banmandaodi Formations in the North) in which
graptolites, dacryoconarids and corals have
been discovered. The Alengchu F orm ation
consists of grey bedded limestone containing
Nowakia acuaria and corals Squameofavosites aff. cechicus, Lyrielasma chapmani,
Cysticonophyllum cf. dentatum, Stortophyllum cf. subcruciatum in its lower part. In the
upper part of this formation the benthos fos­
sils such as Trilobite of Plagiolaria sp.,
Squameofavosites sp., Thamnopora sp. and
pelagic ones as Anetoceras sp., Teicherticeras

sp., Nowakia sp. have been collected. The
B anm andaodi Form ation comprises mainly
of siliceous rocks, interbeds of conglomerates
and shale containing pelagic fossils from
lower upwards: Nowakia zlichovensis , N.

barrandei, N. cancellata. The D azhongzhai
Form ation in the South consists of fine
grained sandstone, mudstone, shale, carbon­
ate shale, siltstone marls. Some fossils of
Nowakia acuaria, Monograptus yukonensis
have been recorded.
M iddle Devonian occurs only in the
South and consists of diverse kinds of lim e­
stone. The thick M aludong Form ation (1800
m), in its abundant association of Coelenterate has been studied. Some of its species are
Favosites goldfussi, F. placentus, F. halanensis, Thamnopora alta, Thamnopora sp.,
Crassialveolites cavernosus, Tryplasma devoniana, Amphipora sp. The Songjiazhai
F orm ation comprises of grey black lim e­
stone with black siliceous and carbonate shale
interbeds which reach 300 m thickness.
Three levels of the following fossils can be
noted: 1) in the black siliceous shale of the
bottom — Styliolina sp., 2) in the limestone
and shale of the middle level — the benthic
fossils
Leptaena
sp.,
Favosites
sp.,

Squameofavosites mironovae, 3) in the upper
level of carbonate and siliceous shale with
limestone interbeds —Styliolina sp., Leptaena
sp. and Nowakia otomari.
Upper Devonian is characterized by two
different facies. In the North the unnamed
formation of Middle and Upper Devonian
(850 m thickness) consists of shale, siliceous
rocks, silicified limestone and fine-grained
sandstone. The fossils are rare, only some
remains of Tentaculites were found. In the
South an unnamed formation of Upper Devo­
nian (400 - 900 m thickness) consists of grey
bigenic limestone bearing benthic fauna such
as Brachiopods — Tenticospirifer vilis, Athyris sp., Corals —Keriophyllum heterophylloides, Disphyllum cylindricum, Tabulophyllum
sp.
In the M id-W est — The Devonian in
Baoshan-Shidan zone is well exposed with
most complete sequences and rich in benthic
fauna.
*In Northwestern area of Việ t Nam a similar as­
sociation has been collected in the equivalent
beds of the level of Nowakia zlichovensis (TDT).

25


Lower Devonian comprises of three
lithostratigraphic formations, namely Xiangyangsi, Wangjiacun and Shabajiao. The first
two formations are assigned to Lochkovian

and Pragian. They consist of grey-green, red­
d is h shale, siltstone, sandstone, marl and
nodular limestone, yielding mainly pelagic
fauna. In the X iangyangsi F orm ation fol­
lowing fossils have been reported — Graptolite: Monogratus cf. uniformis, M. microdon,
M. praehercynicus, Dacryoconarids: Nowakia
intermedia, N. bohemica, N. acuaria, Conodonts: Caudicriodus woschmidti, Brachiopods: Lissatrypa leprosa, Clorinda sp. In the
W angjiacun F orm ation: Monograptus yukonensis, M. aequabilis and Polygnathus dehiscens. Further-more, from here some plant
remains of Zosterophyllum sp., Hostimella sp.
have been identified. The presence of the lat­
ter plant fossils shows the turbidite facies of
the Wangjiacun Formation.
From
the
S h abajiao
Form ation
(Emsian) upwards the platform carbonate fa­
cies is predominant in the sequences with di­
verse kinds of limestone. Some remains of
Polygnathus nothoperbonus are reported from
the Shabajiao Formation.
M iddle Devonian comprises of two for­
mations namely Xibiantang (70 - 100 m
thickness) and Malutang (88 m thickness).
The X ibiantang F orm ation is the first and
lower unit which consists of grey micritic
limestone, calcareous mudstone bearing
Brachipods of Strophochonetes sp., Conodonts of Polygnathus costatus costatus, P.c.
patulus, P.c. partitus, Icriodus retrodepressus. The M alutang F orm ation can be di­
vided into two parts, the lower one consists of

marl, calcareous mudstone and lenses of
limestone yielding Strophoc nonetes sp. and
Corals of Metrionaxon sp., Barrandeophyllum sp. Limestone is the dominant compo­
nent of the upper part, some interbeds of cal­
careous mudstone are also observed. Benthic
faunas are abundant such as Brachiopods of
Emanuella inflata, Bifidia lepida, Aulacella
eifeliensis, Reticulariopsis eifeliensis, Athyris
concentrica, Mesodouvillina sp., Iridistrophia sp.

26

M iddle and Upper D evonian.
The H eyuandai F orm ation (200 - 300
m thickness). Grey light bedded limestone is
the unique component of this Formation and
abundant benthic fossils have been reported
from different level of it. The lower level
contains Brachiopods of Aulacella eifeliensis,
Fitzroyella angularis, Devonaria minuta,
Kayserella lepida, Kerpina viata, Indospirifer
padaukpinensis, Corals of Heterophrentis
yunnanensis, Acanthophyllum sp. In the
middle level Brachiopods are the most abun­
dant with lo.ver diversity, the prevailing spe­
cies are Carinifera transversa, Pyramidalia
paoshanensis, Gypidula sp. No typical Conodonts were recorded and it is difficult to as­
sign this level to Middle or Upper Devonian.
Upper level contains Devonoproductus sp.,
Pugnoides sp., Spinatrypa sp. belonging un­

doubtedly to Upper Devonian.
The D ujacun G roup (200 m thickness)
of limestone and dolomitic limestone is as­
signed to Upper Devonian. Fossils are sparse,
only some poor remains of Tenticospirifer
sp., Disphyllum sp., Amphipora sp., Stromatoporella sp. have been reported.
The uppermost exposure of Upper De­
vonian in this zone is a thin siliceous bed less
than 5m thick which is in disconformity with
the overlying Lower Carboniferous.
NORTH THAILAND (Table 4)
Lower Devonian shale, chert and occa­
sional limestone are outcropped in North
Thailand between Chieng Mai and Fang.
From here Graptolites have been recorded -Monograptus hercynicus, M. aequabilis notoaequabilis, M. yukonensis fangensis and the
Brachiopods of Paterula bohemica were col­
lected in association with M. aequabilis notoaequabilis (Jaeger H. et al. 1969). In the
Mae Ping Formation consisting of thin and
middle bedded limestone in Northwest Thai­
land, south of Chieng Mai, beyond of East
Burma an association of Silurian - Lower De­
vonian Conodonts has been recorded: Belodella s., Panderodus sp., Ozarkodina exclava (Burrett
et al. 1986).

c.


27
Table 4. Devonian stratigraphic units of Shan - Thai terrane

- The data on Middle Devonian in North
Thailand are very sparse. Only some Brachiorotunda
pod
remains
of Swaicoelia
(Ambocoeliid) were recorded from the suc­
cession of shale, sandstone, mudstone in
Fang - Chieng Mai region (Hamada, 1968).
The bearing beds of this Ambocoeliid are "a
portion of the Upper Silurian-Devonian series
of clastics" and Hamada (1968) presumed that
the fauna indicates a "post Middle Devonian"
age for the beds.
- The evidence on the presence of the
Upper Devonian rocks in North Thailand is
very weak. Only along the highway from
Chieng Mai to Fang in the succession of
shale, red mudstone and sandstone Hamada
(1968) described the Brachiopod fossils of
Swaicoelia rotunda and Ambocoeliid indet.
The latter author hesitated to identify the age
of the beds bearing this fauna. From the pa­
laeontological point of view, it is reasonable
to presume that this fauna indicates a post
Middle Devonian age for the beds, he wrote.
But in the end he limited the age of these
beds to Upper Devonian if not Lower Carbon­
iferous.
NORTHWEST THAILAND AND SHAN

STATES OF BURMA
The data on Devonian in this region are
also sparse (Table 4).
- Lower Devonian is not well known in
both Western Thailand and Shan states of
Burma. The graptolitic Zebingyi beds in
Burma contain mainly Silurian fauna but
some Dacryoconarids closed to the Bohemian
forms indicate the presence of Lower Devo­
nian in these beds. The knowledge on the re­
lation of the Zebingyi beds and the Devonian
"Plateau limestone" in the Shan States is not
enough for us to illustrate the SilurianDevonian stratigraphic succession in this area.
In Northwest Thailand (South of Chieng
Mai not far from the Thailand-East Burma
frontier) the Mae Ping Formation consists of
thin and middle bedded limestone bearing
Silurian-Lower Devonian Conodonts: Bellodella sp., Panderodus sp., Ozarkodina excavata. It is still unclear that whether this

28

formation could be an equivalence of the
graptolitic Zebingyi beds in Burma?
M iddle Devonian (and Emsian?) in
this area is well known with the "Plateau
Limestone" in the Shan States of Burma. The
abundant Coral and Brachiopod assemblages
of the "padaukpinensis fauna" were consid­
ered as Eifelian in age by Reed (1908), An­
derson et al. (1969). The latter authors have

suggested
that
the
Brachiopods
of
"padaukpinensis fauna" have affinities with
the "tonkinensis fauna" in South China and
North Việ t Nam. The Coral assemblage of
"padaukpinensis fauna", its age and its bio­
geographic affinities have been re-assessed by
Wright (1995). The study of W right shows
that the padaukpinensis fauna is EmsianGivetian in age and its close affinities with
the European one are well proved.
Upper Devonian in this area is still
poorly studied. There is only the information
on the presence of the Late Famennian (or
early Early Carboniferous?) fish remains from
the limestone in Northwest Thailand, near
Thailand-Burma boundary (Long, Burrett,
1989).

PENINSULA THAILAND AND
MALAYSIA (Table 4)
Many fossils of the age from Ordovician
to Devonian have been described in the pen­
insula Thailand and Malaysia by Japenese
authors. The difficulties are that the succes­
sions of deposits bearing these fossils are not
clear enough for us to assign definitely the
Devonian divisions.

- Lower Devonian took place in the Up­
per Detrital Member which consists of argil­
laceous limestone and interbeds of mudstone.
The Lochkovian-Pragian fauna has been re­
ported such as Nowakia acuaria, leriodus
worschmidti, Monograptus uniformis and
some Brachiopods.
- The Emsian - Middle Devonian suc­
cession present itself the clastics of the Kroh
Plagiolaria Horizon, Bailing Formation and
Stringocephalus perakensis in the higher
level. .The Trilobites Plagiolaria plagiophthalma, PI. potthai have the close


affinities with the European ones. These af­
finities are observed as well in the Brachiopod
assemblage which consists of Baroisella sp.,
Orbiculoides tarda, Plectodonta pacifica, PI.
burtonae, Protochonetes sp., Perakia undulata, Ambocoeliids, etc. Hamada (1969) has
suggested an early Middle Devonian age for
this Brachiopod assemblage.
It is worth noting that a unique, assem­
blage of heterochronic Trilobự es has been
described by Kobayashi and Hamada (1972)
from Devonian rocks of West Malaysia. Most
of them are the endemics such as Pseudotri­
nodus aenigma, Plagiolaria potthai, Bladodalmanites nubelania, Bl. kokesiformis,
Perakaspis
trapezoides,
Perakaspis

(Krohbole) elongata, Perakaspis (Krohboléì)
burtoni, Bailielloides inexpectans, Harpes
(s.l.) kylindrorhachis and others. These fos­
sils. are usually found in associate with the
Lower Devonian Nowakia acuaria, but the
ages of these Trilobites are very different.
Some of them are close to the Ordovician,
others — Devonian Trilobites in other regions
(Kobayashi and Hamada 1972). In spite of
that this fauna is important for the biogeographical analysis. In the generic level this
Trilobite fauna has the affinities with the
European and especially with the Bohemian
ones. The Devonian Plagiolaria is close to
the one of North Việ t Nam (Plagiolaria orientalis), in addition the Dacryoconarids are
the ones of Bohemian.
The Stringocephalus limestone occurs at
Kampar near Ipoh, Perak of West Malaysia.
- The Upper Devonian in this area con­
sists mainly of mudstone of the red-beds
which contain Waribole perlisensis, some
ambocoelids (Swaicoelia rotunda), etc. The
age of this fauna ranges from Late Devonian
to Dinantian (Kobayashi 1973).

REMARKS
1. On the stra tig rap h y and facies
- In most cases of South China, North­
east Việ t Nam areas there is a gap in Silurian
and Lower Devonian boundary sequences.
The lowermost formation of Lower Devonian

consists of the rocks of "Old Red Sandstone"

facies — Lianhuashan Formation in South
China, Sika Formation in Northeast Việ t
Nam. A similar formation takes place in the
Mid-Central Việ t Nam — Tân Lâm Forma­
tion.
- The continuous Silurian - Devonian
boundary can be observed in the Sông Cả
Sections (North of Central Việ t Nam and
Northeast Laos of Indochina terrane), in West
Yunnan; North and Northwest Thailand - East
Burma; in Peninsula Thailand and Malaysia.
In most cases of these sections the Lower De
vonian consists mainly of shale, mudstone
with more or less mixture of carbonate com
ponents containing pelagic fauna (Huổ i Nhj
Formation in North of Central Việ t Nain and
Northeast Laos, Upper Detrital M ember in
Malaysia, Mae Ping Formation in West
Thailand, Zebingyi beds (?) in Burma, Fang
chert in North Thailand and Xiangyangsi
Formation in West Yunnan, etc).
- The Middle Devonian (some time from
Emsian) in most cases is characterized by
fossiliferous carbonate facies. A short gap
took place in the interval o f Middle Devonian
in Northeast Việ t Nam and South China.
- The continuous Devonian - Carbonifer­
ous boundary can take place in South China

(for example Nanbancun section in Guangxi),
North Việ t Nam and in some section of Indo­
china terrane, for example in East Thailand,
in Central Việ t Nam. Meanwhile a clear gap
is noted in West Yunnan, North Thailand and
others.
2. T he endem ism of Low er Devonian fau­
nas in South C hina - N orth Việ t Nam terran e and the southern lim it o f th eir d istri­
bution.
- The high endemism of the Lower De­
vonian faunas in South China and North Việ t
Nam is recorded in both Vertebrate and Inver­
tebrate communities. A great number of en­
demic Brachiopod, Coral and other Inverte­
brate genera and species have been reported
by geologists even in the first decade of the
current century. The first evidence of this en­
demism is the peculiar components of the
well known tonkinensis faunas which con­
tains agreat number of the endemic species
and genera such as the representatives of
29


Echyropora, Solypetra, Mansuyphyllum, Euryspirifer, Dicoelostrophia, Parachonetes,
Gracicalymene, Pỉ agiolaria, Ductina and
others. The endemism of the Lower Devonian
fauna in South China and North Vietnam is
especially expressed in the famous Vertebrate
community. Numerous genera of Galeaspid,

Yunnanolepiforra and others are up to now
found only in this region of world.
- A part from the high endemism, the af­
finity of Devonian Invertebrates of South
China and North Việ t Nam with the European
ones is clear. Remarkable are the species of
genera — Atelodictyon, Clathrocoilona,
Clavidictyon, Ferestromatopora, Flexiostroma,
Gerronostroma,
Hermatostroma,
Idiostroma, Parallelostroma, Plectostroma,
Praeidiostroma, Salairella, Simplexodictyon,
Stelodictyon, Stictostroma, Syringostromella,
Tienodictvon, I rupestostroma, etc. of Strom atoporoid,
Emmonsia,
Riphaeolites,
Gracitopora, Roemeripora, Tyrganolithes,
Podolites, Chaetetipora, etc. of T abulate,
Cyathactis, Cylindrophvllum, Cystophrentis,
Evenkieha, Glossophyllum, Kuangxiastraea,
Lindstromella, Mansuvphyllum, Nalivknella,
Parazelophyllia, Phollidophyllum, Pseudogrypophyllum, Pseudotryplasma, Sinospongophyllum, Solipetra,
etc. of Rugoses,
Acrospirifer, Athyrisina, Aulacella, Cymostrophia, Dicoelostrophia, Douvillina, Euryspirifer, Glossinotoechia, Gypidula, Howellella, Indospirifer, Leptaena, Leptaenopvxis, Levenella, Meristella, Mucrospirifer,
Nervostrophia, Protathyris, Pugnacina, Thiemella, Undispirifer, etc. of Brachiopods,
Mvtilarca, Pteria (Actinopteria), Pterinea
(Fterinea), Pterinea (Cornellites), Pterinea
cTolmaia ), etc. of Bivalvia, Gracica'ymene,
Proetus, Plagiolaria, Ductina, etc. of T rilobites.
- In tectonic aspect the Red River (Sông

Hồ ng) stripe-slip fault is considered by many
authors as the south limit of the South China
terrane or block. But the paleontological data
obtained daring the last decades show that the
Sông MS fault, but not the Red River one,
plays an important role in the distribution of
the Devonian fauna. The representatives of
the Euryspirifer tonkinensis are widespread in
30

both sides of the Red River fault of North
Việ t Nam. Recently the similarity of the
Lower Devonian fauna in both sides of the
Red River fault is also proved by the discov­
ery of a "South Chinese" Vertebrate fauna
from the Lower Devonian of the Lower Sông
Đà River (Janvier et al. 1996).
The dissimilarity of the Lower Devonian
fauna of die North and the Central Việ t Nam,
that are in two sides of the Sông Mã fault,
was noted by one of us (TDT) in 1965. Up to
now the Euryspirifer tonkinensis fauna has
not bean found in the South from the Sông
Mã fault.
From the above mentioned data, in our
opinion the Sông Mã fault must play such a
role as the southern lim it of the South China
and North Việ t Nam terrane.
3. T he E uropean - B ohem ian affinities of
the Devonian faunas in Southeastern Asia.

- The. affinity of Devonian Invertebrates
of South China and North Việ t Nam with the
European ones is proved in above paragraph.
- Devonian fauna of the Indochina terrane is rather different from the one of South
China and North Việ t Nam terrane. Like in
Central Việ t Nam, the main representatives of
the tonkinensis fauna are not found in the
whole territory of the Indochina terrane.
Meanwhile, in the Devonian fauna of this terrane the European representatives and cos­
mopolites are common. Apart from the pe­
lagic cosmopolite fauna, numerous Europeanlike fossils have been reported in this tcrrane.
Among them the known species and genera
are Corals — Favosites goldfussi, Fav. styriacus, Fav. ottiliae, Heliolites porosus, Alveolitella densata, Gracilopora polonica,
Caliapora baitersbyi, Chaeteies inflatus,
Phillipsastraea hennahi, Endophyllum abditum, Thamnophyllum stachei, Dendrostella
rhenana and other species of the genera
Cyathactis, Cylindrophyllum, Evenkiella,
CAossophyllum, Lindstromella, Nalivknella,
Parazelophyllia, Phollidophyllum, Pseudogrypophyllum, Pseudotryplasma, Pseudogrypophyllum,
Spongophyllumand
others,
Brachiopods — species of Schizospirifer,
Schizophoria,
Mucrospirifer,
Athyris,


weak evidence for a conclusion that a part of
Gypidula, Cyrtospirifer, Cyrtiopsis and oth­
these

terranes was derived from Gondwana.
ers.
One of us (NHH) has counted the species
A cknow ledgm ent. This paper is com­
of the main Devonian invertebrate groups
pleted in the framework of the IGCP Project
from Centrạ l Việ t Nam. As a result the ma­
306 and the Vietnamese Fundamental Science
jority of thèm is in common with the Euro­
Research Project 7.2.6. Thanks to the kind­
pean and Southern Chinese (64% of Stroness of Dr. Philippe Janvier (Institut de
matoporoids, 70% of Brachiopods and 75%
Paléontologie de Paris) the senior author was
of Corals). There are only a few common
able to have the favorable conditions for the
forms with Australian (3% of Stroconsultation with the publications in the Li­
raatoporoids, 3,8% of Brachiopods and 8% of
braries of Paris. We are grateful to Dr. VŨ
Corals).
Devonian fauna of Shan - Thai terraneNgọ c Tú (Việ t Nam National University, Ha­
noi) who reviewed the English text and gave
also has a remarkable affinity with the Euro­
his help in the improvement of the paper
pean one. The closeness of the padaukpinenmanuscript.
sis and tonkinensis faunas has been noted by
Anderson et al. (1969), both two of them are
close to the European ones (Wright 1996).
R E FER E N C E S
Hou Hong-fei and Wang Shitao (1996)
have given a special analysis on Devonian

HOUCOT A.J., JHONSON J.G. & TALENT J.A.
fauna of West Yunnan. The main Lower and
1969.
Early
Devonian
Brachiopod
Middle Devonian Brachiopod genera are
Zoogeography.
Geol.
See.
America.
Spcial
Athyris, Aulacella, Bifida, Canplioplia,
paper
119:11
Opgs
Carinifera, Emanuella, Eoreticulariopsis,
BUNOPAS S. 1992. Regional Stratigraphie Cor­
Fitzroella, Gypidula, Kerpina, Indospirifer,
relation in Thailand. Proceed. Nat. Confer,
Iridistrophia,
Kayserella,
Lyssatrypa,
on Geol. Res. of Thailand. Supl. Vol. : 198Mesodouvillina, Plectodonta, Pyramydalia,
208. Bangkok.
Spinatrypa, Strop hoc honetes, Yunnanlepta.
BUNOPAS S. 1994. The regional stratigraphy,
This fauna is basically identical with those of
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