名古屋大学博物館報告
Bull. Nagoya Univ. Museum
No. 28, 27–38, 2012

Description of sandstones in the Ulaanbaatar area, Mongolia.
Toshiya Suzuki1), Yuki Nakane1), Bakhat Nuramkhaan2),
Makoto Takeuchi1), Kazuhiro Tsukada3), Sersmaa Gonchigdorj2),
Khishigsuren Sodnom2) and Manchuk Nuramkhaan2)
1) Graduate School of Environmental Studies, Nagoya University, Nagoya 464-8602, Japan
2) School of Geology and Petroleum Engineering, Mongolian University of Science and Technology, Ulaanbaatar,
Mongolia
3) Nagoya University Museum, Nagoya 464-8601, Japan

Abstract
The texture and the grain composition of sandstone provide information about the tectonic setting of basinsof deposition and associated provenances. The geological history of the Khangay-Khentey belt composed of
pre-Carboniferous accretionary complex and Carboniferous shallow-marine strata was linked with the evolution of the Mongol-Okhotsk Ocean. This paper describes the sandstones of the Gorkhi, Altan-Ovoo & OrgiochUul Formations and Carboniferous shallow marine system, that occurs around Ulaanbaatar city
The sandstones in the Gorkhi and Altan-Ovoo & Orgioch-Uul Formations are classified as feldspathic
arenite. They are clast supported and poorly-sorted, with dominantly angular to very angular grains mainlycomposed of quartz, potassium feldspar, plagioclase and rock fragments of rhyolite and tuff. The modal
framework grain analysis shows that sandy detritus was derived from “continental crust” where erosion has
cut deep into volcanic cover. The sandstone in the Carboniferous shallow marine system classified as feldspathic wacke is rich in muddy matrix and poorly-sorted, dominantly includes rounded to little angular grainsof quartz, potassium feldspar, plagioclase and rock fragments of rhyolite, felsic tuff, andesite and basalt. The
Qm-F-Lt diagram suggests that the sandstone is originated from the “transitional arc”.
The sandstones from the Gorkhi and Altan-Ovoo & Orgioch-Uul Formations are significantly similar andthey can not be distinguished to each other in their textures, grain compositions and poor in rock fragments,
and they were originated from the same kinds of source, i.e. continental crust where erosion has cut deep into
volcanic cover which related to the subduction of oceanic plate. However, the lithostratigraphies of theseformations are quite different each other and they were likely to have been formed at different places, or formed
in different ages each other. The volcanism evidenced by the felsic tuff intercalations in the Altan-Ovoo &Orgioch-Uul Formation at the provenance area was likely enough immature which could not provide much
volcanic rock fragments to the basin. The sandstone of the “Carboniferous formation,” rich in volcanic rockfragments, strongly indicates that the volcanic activity had developed to supply volcanic rock fragments into
the sedimentary basin of this formation.

1. Introduction
The Mongolian territory lies in the heart of the Central Asian Orogenic Belt (CAOB), that developed
between the Angara craton to the north and the North China and Tarim blocks to the south (Fig. 1).
Tectonic history of the CAOB has important implications for the growth mechanisms of continental crustin Earth’s history (Kovalenko et al., 2004). Sengör and Natal’in (1993) envisaged that the KhangayKhentey belt, central Mongolia (Fig. 2), has been formed by closer of the Mongol-Okhotsk Ocean between
the Angara craton and the North China block; however its closure process and tectonic setting are still
debated (e.g. Enkin et al., 1992; Zorin et al., 1993). The provenance analysis of the Khangay-Khentey
belt, which is composed of accretionary complex and Carboniferous shallow-marine strata, would givea contribution to examine the closure process and tectonic setting of this ocean. The texture and graincomposition of clastic rocks let us know the nature of the source rocks in the provenance area which can— 27 —

be depended on their tectonic settings. Consequently, detrital framework modes of sandstone suites
provide important information in considering the tectonic setting of basins of deposition and associatedprovenances. This paper presents microscopic description of the sandstone in the Khangay-Khentey belt
at the Ulaanbaatar area to examine the tectonic setting of this belt.

Fig. 1 Tectonic map of Northeast Asia showing the locations of the Central Asian Orogenic(CAOB) (Kurihara et al., 2008).

Fig. 1 Tectonic map of Northeast Asia showing the locations of the Central Asian Orogenic
Belt (CAOB) (Kurihara et al., 2008).

Fig. 1 Tectonic map of Northeast Asia showing the locations of the Central Asian Orogenic(CAOB) (Kurihara et al., 2008).

Fig. 2 Tectonic division of Mongolia showing the distribution of the Khangay-Khenety
belt (modified from Tomurtogoo, 2003). 1: Central Mongolia superterrane, 2: complex terrane, 3: Mongol Altai orogenic belt, 4: Khangay-Khentey belt, 5: Idermeg
Fig. 2terrane,
Tectonic
division of Mongolia showing the distribution of the Khangay-Khenety
6: Undur haan terrane 7: Gobi Altai-Baruun Urt terrane, 8: Edren terrane,
9: Mandah terrane,
Gurvansaihan terrane,
11:1:
Baruunkhuuraiterrane, 12:superterrane,South(modified
from10:Tomurtogoo,
2003).
CentralMongolia
2: complex terran
Gobi superterrane, 13: Zamiin Uud terrane, 14: Khutag Uul terrane, 15: Sulinheer
and Duulgant
terrane,
16: Main belt,
MongolianLineament fault, 17: Other
faults.
MongolAltai
orogenic
4: Khangay-Khentey
belt,
5: Idermeg terrane, 6: Undur

Fig. 2 Tectonic division of Mongolia showing the distribution of the Khangay-Khenety
terrane
7: from
GobiTomurtogoo,
Altai-Baruun
Urt 1:terrane,
Edren superterrane,
terrane, 9: 2:
Mandah(modified2003).
Central 8:
Mongolia
complexterrane,
terran2. Geological outline in the Ulaanbaatar area

Gurvansaihan
11:belt,
Baruunkhuurai terrane, 12:South
Gobi superterrane,
13: ZahMongolAltaiterrane,
orogenic
4: Khangay-Khentey
5: Idermeg
terrane, 6: Undur
The Paleozoic rocks
in the Ulaanbaatar
area aredividedinto the Gorkhi andbelt,
Altan-Ovoo& Orgiochterrane,
14:
terrane,SulinheerandDuulgant
terrane,
16: Mainterrane,
Mong
Uul Formations of Uud
accretionary
andUulthe Carboniferous
shallowsystem(Takeuchietterrane7: complexes
GobiKhutag
Altai-Baruun
Urt15:
terrane,8:marine
Edrenterrane,
9: Mandahal., 2013, Fig. 3).
Lineament
fault,terrane,
17: Otherfaults.
Gurvansaihan
11:
Baruunoccupy
khuurai
12: andSouth
Gobi
superterrane, 13: Zam
The Gorkhi and Altan-Ovoo& Orgioch-Uul
Formations
theterrane,
southeasterneasternto central
parts of this area respectively(Fig.3).
Carboniferous
shallowmarine system“Carboniferous
Uud terrane,
14:TheKhutagUul terrane,
15: Sulinheerand (here,
Duulgant
terrane, 16: Main Mongo
formation”) is distributed in the northwestern part of this area (Fig. 3). Mesozoic Granite (Tomurtogoo

Lineament fault, 17: Other faults.
— 28 —

et al., 1998) intrudes into the Altan-Ovoo & Orgioch-Uul Formation in the southeast area. The Cretaceous
system (Tomurtogoo et al., 1998) composed of white claystone and conglomerate exposed in the northwestof central Ulaanbaatar unconformably covers the rocks of the accretionary complex. The Gorkhi Formationconsists mainly of massive sandstone with small amounts of mudstone, siliceous mudstone and chert.
The chert contains Upper Silurian to Upper Devonian radiolarians (Kurihara et al., 2009; Nakane et al.,2013). The Altan-Ovoo & Orgioch-Uul Formation consists mainly of sandstone, mudstone and alternating
beds of sandstone and mudstone with small amounts of conglomerate, felsic tuff, siliceous mudstone,chert and basalt. The “Carboniferous formation” consists mainly of sandstone and mudstone with small
amounts of conglomerate. The “Carboniferous formation” yields brachiopods (Takeuchi et al., 2013).
The Gorkhi Formation is in fault contact with the Altan-Ovoo & Orgioch-Uul Formation. The Altan-Ovoo& Orgioch-Uul Formation is uncomformably overlain by the “Carboniferous formation” (Takeuchi etal., 2013).
The Gorkhi and Altan-Ovoo & Orgioch-Uul Formations are complexly folded with northeast-trending
sub-horizontal axes (Fig. 3). Northwest-trending faults cut the above three formations to form faultbound-blocks at the northwestern part of the study area (Fig. 3).

Fig. 3 Simplified Geologic map of the Ulaanbaatar area (modified from Takeuchi et al., 2013) with sampling point of
Fig.3 Simplified Geologic map of the Ulaanbaatar area (modified from Takeuchi et al., 2013) with sampling point of the sandstone.
the sandstone.

3. Methodology – classification and modal framework grain analysis of sandstone
Sandstone is divided into wacke and arenite by its matrix quantity. The sandstone can be furthermore
classified into the quartzose arenite/wacke, feldspathic arenite/wacke, and lithic arenite/wacke with theirquantitative ratio of monomineralic quartz (Q), feldspar (F) and polycrystalline lithic fragments (R)(Okada, 1971, Fig. 4a).
In addition, the modal framework grain analysis in sandstone with monomineralic quartz (Qm), feldspar(F) and polycrystalline lithic fragments (Lt) allows the interpretation of the plate tectonic position of thesource terranes divided into continental blocks, magmatic arcs and recycled orogens (Dickinson et al.,— 29 —

1983, Fig. 4b). The “continental blocks” include craton interior, basement uplift where erosion has cut
deep into the continental crust and their transition (Dickinson et al., 1983, Fig. 4b). The “magmatic arcs”
are subdivided into the dissected arc in which plutons are exposed from erosional unroofing, undissected
arc in which volcanic cover present, and their transition (Dickinson et al., 1983, Fig. 4b).
The above two methods, i.e., traditional classification of sandstone (Okada, 1971) and modal analysis
of framework grains (Dickinson et al., 1983) for forty-two medium-grained sandstone samples were
examined in this study. Twenty-four, sixteen, and two samples in which of them were from the Gorkhi,
Altan-Ovoo & Orgioch-Uul, and “Carboniferous” Formations respectively (Fig. 3). Five hundred grains
for each sample were counted using the Gazzi-Dickinson method (Dickinson et al., 1983) in thin sections
stained for potassium feldspar by sodium cobaltinitrite.

(a)

(b)

Fig. 4 (a) Petrographic classification of sandstone (Okada, 1971). (b) Compositional
fields indicative of sandstone derivation from different types of provenance(Dickinson et al., 1983).

Fig.4 (a) Petrographic classification of sandstone (Okada, 1971). (b) Compositional fields indicative
4. Description of the sandstoneof sandstone derivation from different types of provenance (Dickinson et al., 1983).
4.1. Gorkhi Formation
The sandstone of this formation, clast-supported (< 5 % of muddy matrix) and poorly-sorted, dominantly
includes angular to very angular grains of quartz, potassium feldspar, plagioclase and rock fragments ofrhyolite and felsic tuff with lesser amounts of biotite, muscovite, sphene, zircon, epidote, hornblend, chrolite
and rock fragments of sandstone, mudstone, andesite and basalt (Figs. 5a and b). Allanite is rarely present.
— 30 —

Fig. 5 Photomicrographs of sandstone of the Gorkhi Formation, (a): plane polarized light (b): crossed polars, the AltanOvoo & Orgioch-Uul Formation, (c): plane polarized light (d): crossed polars, and the Carboniferous formation,(e): plane polarized light (f): crossed polars. Qtz: quartz, Pl: plagioclase feldspar, Kfs: potassium feldspar, Hbl:
hornblend Rh: rhyolite, Tu: tuff, Ba: basalt, SS:sandstone.

It is classified as feldspathic arenite in the Q-R-F diagram (Okada, 1971, Fig. 6a). According to themodal framework grain quantification, the most of the samples are plotted in the field of “basement uplift”
where erosion has cut deep into the continental crust, and a few samples are plotted in the field of “dissectedvolcanic arc” where erosion has exposed batholiths beneath volcanic cover (Fig. 6b).

— 31 —

4.2. Altan-Ovoo & Orgioch-Uul Formation
The sandstone of this formation, clast-supported (< 3% of muddy matrix) and poorly-sorted, dominantly
includes angular to very angular grains (Figs. 5c and d). It contains quartz, potassium feldspar, plagioclase
and rock fragments of rhyolite and tuff with lesser amounts of biotite, muscovite, sphene, zircon, epidote,chrolite, and rock fragments of sandstone, mudstone, andesite and basalt. Hornblend, allanite andpumpellyite are rarely present.
The present sandstone is classified as feldspathic arenite in the Q-R-F diagram (Okada, 1971, Fig.
6a). The most of the samples are plotted in the field of “basement uplift” of the “continental block” inthe Qm-F-Lt diagram for the modal framework grain quantification (Fig. 6b).
4.3. “Carboniferous formation”
The sandstone of this formation, rich in muddy matrix and poorly-sorted, dominantly includes rounded

(a)

(b)

Fig. 6Fig.6(a) Petrographic
classificationand (b) andmodal
grain quantification(a) Petrographic
classification(b)framework
modal frameworkgrain quantification of the sandstonesof the sandstones in the Gorkhi and Altan-Ovoo & Orgioch-Uul Formationsin the Gorkhi and Altan-Ovoo & Orgioch-Uul Formations and Carboniferous formation.
and Carboniferous formation.
— 32 —

to little angular grains of quartz, potassium feldspar, plagioclase and rock fragments of rhyolite, felsic
tuff, andesite and basalt with lesser amounts of biotite, muscovite, chrolite, zircon, and rock fragmentsof sandstone and mudstone with 20 to 25% of muddy matrix (Figs. 5e and f). Allanite and augite arerarely included in.
It is classified as feldspathic wacke in the Q-R-F diagram (Okada, 1971, Fig. 6a). The Qm-F-Lt diagramsuggests that the sandstone is originated from the “transitional volcanic arc” which is intermediate between
the dissected and undissected arcs (Fig. 6b).
5. Discussion
The sandstones from the Gorkhi and Altan-Ovoo & Orgioch-Uul Formations are significantly similar
and they can not be distinguished to each other in their textures, grain compositions and poor in rockfragments (Figs. 5, 6, and 7, Table.1). Moreover, they are plotted in the same field of the “basement uplift”
in the Qm-F-Lt diagram for the modal framework grain quantification (Fig. 6b). In addition, the sandstones

Fig. 7 The proportion of minerals and rock fragments in sandstones of the Gorkhi and Altan-Ovoo & OrgiochUul
Formations
and Carboniferous
formation.
Fig.7
The proportionof minerals and rockfragments in sandstones of the Gorkhi and Altan-Ovoo &Orgioch-Uul Formations and Carboniferous formation.

— 33 —

Table. 1 Point-count data for the sandstones of the Gorkhi Formation (a), the Altan-Ovoo & Orgioch-Uul Formation (b)and the Carboniferous formation (c).

(a)
rock No

quartz (%)

K-feldspar (%)

plagioclase (%)

heavy minerals (%)

rock fragments (%)

1
2
3
4
5
6
7
8
9
10
11
12
13
14
15
16
17
18
19
20
21
22
23
32

27.6
34.6
29.4
35.6
25.0
27.0
46.8
37.8
31.0
28.4
28.4
30.0
23.0
34.8
19.8
26.6
26.4
23.5
31.4
38.8
29.9
36.6
27.8
15.3

17.4
10.8
15.6
24.8
5.8
9.0
7.2
12.2
9.0
10.2
22.8
17.6
11.8
9.4
14.0
14.8
8.4
9.2
12.8
11.0
13.0
8.8
12.7
14.5

37.0
28.0
33.6
25.0
35.6
48.0
25.2
34.0
45.4
35.4
28.2
30.0
46.8
28.0
44.8
36.4
44.2
45.8
32.6
26.6
48.5
31.2
48.8
57.8

6.4
8.2
6.2
8.0
5.6
5.2
1.0
4.6
1.4
11.4
7.6
8.4
6.0
6.4
8.8
14.4
7.8
4.3
11.6
6.4
2.6
7.8
4.9
2.4

11.6
18.4
15.2
6.6
28.0
10.8
19.8
11.4
13.2
14.6
13.0
14.0
12.4
21.4
12.6
7.8
13.2
17.2
11.6
17.2
6.0
15.6
5.9
10.0

rock No

quartz (%)

K-feldspar (%)

plagioclase (%)

heavy minerals (%)

rock fragments (%)

24
25
26
27
28
29
30
31
33
34
35
36
37
38
39
40

32.2
32.9
25.8
22.5
31.6
28.6
20.3
26.7
42.3
33.9
29.0
30.5
37.3
26.8
27.1
33.1

11.9
17.6
12.3
12.7
10.3
12.4
10.8
11.5
14.1
7.5
6.2
14.1
7.7
8.7
10.9
7.4

44.5
41.9
47.9
50.8
43.4
41.8
58.2
43.1
27.4
39.3
48.5
38.0
37.7
45.7
48.9
42.8

2.2
1.2
3.4
5.6
2.6
3.1
4.4
3.6
2.2
2.4
2.6
2.8
2.8
5.7
2.8
1.9

9.3
6.4
10.7
8.4
12.0
14.1
6.2
15.0
14.1
16.9
13.7
14.5
14.5
13.0
10.3
14.8

quartz (%)
19.8
13.6

K-feldspar (%)
9.8
9.2

plagioclase (%)
32.2
35

heavy minerals (%)
2.6
0.6

rock fragments (%)
35.6
41.6

(b)

(c)
rock No41
42— 34 —

(a)

(b)

(c)

Fig. 8 Schematic illustrations of inferred sedimentary environments of the Gorkhi
Formation (a), the Altan-Ovoo & Orgioch-Uul Formation (b) and theCarboniferous formation (c).

Fig.7 Schematic illustrations of inferred sedimentary environments of the Gorkhi Formation (a), the& Orgioch-Uul
Formation(b)andandca.
the400Carboniferous
formation(c). Keltyof these formationsAltan-Ovoo
have same age-peaks,
ca. 340
to 350 Ma
Ma (Bussien
et al., 2011;
et al., 2008), of detrital zircons. These facts suggest that the sandstones of these formations were originatedfrom the same kinds of source, i.e. continental crust where erosion has cut deep into volcanic cover which
related to the subduction of oceanic plate (Figs. 8a and b). However, the lithostratigraphies of theseformations are quite different each other. The Gorkhi Formation is dominant in thick massive bedded— 35 —

— 36 —

Qtz: point-countquartz, Kfs:
potassium
feldspar,ofFld:
plagioclase
feldspar, &FVo:
felsic volcanicrock,andesite, Ba:formation.
basalt, SS:
Table. 2formation.
Representative
data
for the sandstones
the Gorkhi
and Altan-Ovoo
Orgioch-Uul
Formations
andAnd:the Carboniferous
Qtz:sandstone,
quartz, Kfs:MS:
potassium
feldspar,Fld:plagioclase
feldspar,FVo:
felsicvolcanicrock,And:
andesite,Ba:
basalt,SS:
sandstone,MS:
mudstone,Bt:
biotite,Chl:chlorite,Ep:
epidote,Ms:
muscovite,
mudstone, Bt: biotite, Chl: chlorite, Ep: epidote, Ms: muscovite, Spn: sphene, Zrn: zircon, Hbl: hornblend
Spn: sphene, Zrn: zircon, Hbl: hornblend

Table.2 Representative point-count data for the sandstones of the Gorkhi and Altan-Ovoo & Orgioch-Uul Formations and the Carboniferous

sandstone, on the other hands the Altan-Ovoo & Orgioch-Uul Formation is largely occupied by mudstonerich strata with felsic tuff intercalations (Takeuchi et al., 2013). Although it is difficult to make an accurate
discussion because there is no information about the age of their sedimentation, this fact may show thatthese formations had been formed at different places, or formed in different ages each other.
The poorness of the volcanic rock fragments in the Altan-Ovoo & Orgioch-Uul Formation suggestthat less volcanic rocks had been exposed at the provenance area to provide it into the sedimentary basin(Fig. 8b, Tables 1 and 2). The volcanism evidenced by the felsic tuff intercalations in the Altan-Ovoo &Orgioch-Uul Formation at the provenance area was likely enough immature which could not provide
much volcanic rock fragments (Fig. 8b).
The “Carboniferous formation” yielding brachiopod fossils unconformably overlies the Altan-Ovoo& Orgioch-Uul Formation. It indicates that the Altan-Ovoo & Orgioch-Uul Formation had already been
exposed when the “Carboniferous formation” was formed (Fig.8c). The sandstone of the “Carboniferous
formation” is rich in volcanic rock fragments (Fig.7, Table.3). The modal framework grain quantification
by Qm-F-Lt diagram suggests that the sandstone of this formation is originated from the “transitionalarc”. It strongly indicates that the volcanic activity had developed to supply volcanic rock fragments into
the sedimentary basin of the “Carboniferous formation” (Fig. 8c).
Acknowledgements
We wish to thank the all staffs and students at the Mongolian University of Science and Technology
involving our field research for their helpful support. Special thank goes to Dr. Sersmaa Gonchigdorj forarrangement of our study. This work was supported by Grant in Aid for scientific research by the Ito
Kagaku Shinko-kai and the Japan Society for the Promotion of Science (No. 20403013), Grant in Aidfor JSPS Fellowship (No. 02087), and the Socho-Sairyo-Keihi of the Nagoya University, Japan.
References
Bussien, D., Gombojav, N., Winkler, W. and Quadt, A. (2011) The Mongol-Okhotsk Belt in Mongolia — An appraisalof the geodynamic development by the study of sandstone provenance and detrital zircons. Tectonophysics, 510, 132150.
Dickinson, W.R, Beard, L.S., Brakenridge, G.R, Erjavec, J.L., Ferguson, R.C., Inman, K.F. (1983) Provenance of North
American Phanerozoic sandstones in relation to tectonic setting. Geological Society of America Bulletin, 94(2),222–35.
Enkin, R.J., Yang, Z.Y., Chen, Y., Courtillot, V. (1992) Paleomagnetic constraints on the geodynamic history of China
from the Permian to the present. Journal of Geophysical Research, 97, 13, 953-13, 989.
Kelty, T.K., Yin, A., Dash, B., Gehrels, G.E. and Ribeiro, A.E. (2008) Detrital-zircon geochronology of Paleozoic sedimentary rocks in the Hangay—Hentey basin, north-central Mongolia: Implications for the tectonic evolution of theMongol—Okhotsk Ocean in central Asia. Tectonophysics, 451, 290-311.
Kovalenko, V.I., Yarmolyuk, V.V., Kovach, V.P., Kotov, A.B., Kozakov, I.K., Salnikova, E.B., Larin, A.M. (2004) Isotope
provinces, mechanisms of generation and sources of the continental crust in the Central Asian mobile belt: geologicaland isotopic evidence. Journal of Asian Earth Sciences, 23, 605-627.
Kurihara, T., Tsukada, K., Otoh, S., Kasiwagi, K., Minjin, ch., Dorjsuren, B., Bujinlkham, B., Sersmaa, G., Manchuk,N., Niwa, M., Tokiwa, T., Hikichi, G., Kozuka, T. (2009). Upper Silurian and Devonian pelagic deep-water radiolarian chert from the Khangai-Khentei belt of Central Mongolia: Evidence for Middle Paleozoic subduction-accretion
activity in the Central Asian Orogenic Belt. Journal of Asian Earth Sciences, 34, 209-225.
Nakane, Y., Bakht, N., Kurihara, T., Manchuk, N., (2013) Lower Devonian radiolarian chert from the Orgioch Formation
at southeast of Ulannbaatar (Gachuunt-Nalaikh), central Mongolia. Bulletine of the Nagoya University Museum,No.28, 19-26.
Okada, H. (1971) Classification of Sandstone: Analysis and Proposal. The Journal of Geology, 79(5), 509-525
Sengöl, A.M.C., Natal’in, B.A. and Burtman, V.S. (1993 Evolution of the Altaid tectonic collage and Palaeozoic crustal
growth in Eurasia. Nature, 364, 299-307.

— 37 —

Takeuchi, M., Tsukada, K., Suzuki, T., Nakane, Y., Sersmaa, G., Manchuk, N., Kondo, T., Matsuzawa, N., Bacht, N.,
Khishigsuren, S., Onon, G., Katsurada, Y., Hashimoto, M., Yamasaki, S., Matsumoto, A., Oyu-Erdene, B., Bulgantsetseg,
M., Kundyz, S., Enkhchimeg, L., Ganzorig, R., Myagmarsuren, G., Jamiyandagva, O., Molomjamts, M. (2013)
Stratigraphy and geological structure of the Paleozoic system around Ulaanbaatar, Mongolia. Bulletine of the Nagoya
University Museum, No.28, 1-18.
Tomurtogoo, O., Byamba, J., Badarch, G., Minjin, Ch., Orolmaa, D.,Khosbayar, P. and Chuluun, D. (Eds.) (1998) Geologic
map of Mongolia, Scale 1:1,000,000 and summary. Mineral Resources Authority of Mongolia, Ulaanbaatar.
Tomurtogoo, O. (2003) Tectonic Map of Mongolia at the scale of 1:1,000,000, and Tectonics of Mongolia (Brief explanatory notes to Tectonic of Mongolia at the scale of 1:1,000,000). Mineral Resources Authority of Mongolia,
Ulaanbaatar.
Zorin, Yu.A., Belichenko, V.G., Turutanov, E.Kh., Kozhevnikov, V.M., Rushentsev, S.V., Dergunov, A.B., Filippova, I.B.,
Tomurtogoo, O., Arvisbaatar, N., Bayasgalan, Ts., Biambaa, Ch. And Khosbayar, P. (1993) The South Siberia-Central
Mongolia transect. Tectonophysics, 225, 361-378.

（2012 年 10 月 15 日受付，2012 年 12 月 25 日受理）

— 38 —