名古屋大学博物館報告
Bull. Nagoya Univ. Museum
No. 28, 19–26, 2012

Geological division of the rocks at southeast of Ulaanbaatar(Gachuurt-Nalaikh), central Mongolia
Yuki Nakane1), Toshiyuki Kurihara2), Bakhat Nuramkhaan3),
Manchuk Nuramkhaan3), Makoto Takeuchi1), Kazuhiro Tsukada4),
Sersmaa Gonchigdorj3) and Khishigsuren Sodnom3)
1) Graduate School of Environmental Studies, Nagoya University, Chikusa-ku, Nagoya, 464-8601, Japan
2) Graduate School of Science and Technology, Niigata University, Igarashi 2-no-cho, Nishi-ku, Niigata, 9502181, Japan
3)	School of Geology and Petroleum Engineering, Mongolian University of Science and Technology, Ulaanbaatar,Mongolia4) Nagoya University Museum, Chikusa-ku, Nagoya, 464-8601, JapanAbstract
This paper describes lithology and radiolarian fossils from a chert slab in the Gachuurt-Nalaikh area,
southeast of Ulaanbaatar, central Mongolia, and discusses the geological division of the rocks in this area.
The rocks in this area consist of clastic rocks with chert slab intercalations. Although the rocks of this area
have been previously divided into the Gorkhi, Altan-Ovoo, and Orgioch-Uul Formations, there are no significant structural and lithological gaps across the boundaries between these formations. Therefore, there is
no reason to divide the rocks of this area into the three formations, and these three formations should be regarded as a single geological unit.
A conformable succession of Devonian radiolarian chert, siliceous shale, mudstone and sandstone in ascending order, which is generally regarded as ocean plate stratigraphy (OPS), were found from this area. The
repetition of chert and clastic rocks with OPS within this area might show the stacking of tectonic slices of
the chert-clastic rock sequence within an accretionary complex. This suggests that the rocks of this area should
be regarded as the northern extension of the Gorkhi Formation of an accretionary complex, though most of
the rocks of this area have been previously assigned to Carboniferous shallow marine system.

1. Introduction
The Central Asian Orogenic Belt (CAOB) lies between the Angara craton to the North and the North
China and Tarim blocks to the south, and comprises a number of tectonic zones, which includes someaccretionary complexes. The age and the geological structure of these accretionary complexes are keys
for understanding the forming process of the CAOB.
The Khangai-Khentei belt within the CAOB at central Mongolia is an accretionary complex withCarboniferous shallow marine system (Kurihara et al., 2009). Although lithology and stratigraphy ofthese formations have been examined, little is known about the boundary and relationship between theaccretionary complex and the Carboniferous system (e.g., Kurihara et al., 2009; Minjin et al., 2006).
A geological mapping project between Mongolian University of Science and Technology and Nagoya
University, Japan, have been carried out to reveal the detailed stratigraphy and structure of the accretionary
complex and the Carboniferous system in the Ulaanbaatar area since 2009, and remarkable radiolarianchert slabs were found from the Gachuurt-Nalaikh area through the course of this project. This paper
describes lithology and radiolarian fossils from one of these chert slabs, and discusses the geologicaldivision of the rocks in the Gachuurt-Nalaikh area.

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2. Geological outline of the Khangai-Khentei belt
The Khangai-Khentei belt is distributed, approximately 300 km wide and 1200km long, trending
NE-SW in the central part of Mongolia (Fig. 1). According to Sengör et al. (1993) and Sengör and Natal’in(1996), this belt consists of Neoproterozoic to Lower Cambrian ophiolites and Lower Paleozoic to
Carboniferous turbidites, mafic to intermediate volcanic rocks, and minor chert.

Fig. 1 The tectonic subdivision schema of Mongolia (terranes: Zag-Haraa (ZH), Asralt-Hairhan (AH),
Kharhorin (HH), Tsetserleg (TT), Ulaanbaatar (UB), Onon (ON)) (modified from Tomurtogoo, 2010).

Fig. 1The Khangai-Khentei belt is subdivided into theSilurian Mandal Group (Tomurtogoo et al., 1998),
the Lower Devonian Sergelen Formation, the Middleto Upper Devonian Gorkhi Formation, the Lower
Carboniferous Altan-Ovoo Formation and theLower to Upper Carboniferous Orgioch-UulFormation (Minjin et al., 2006) (Fig. 2).
Tomurtogoo (2010) divided the Paleozoic rocksof the Khangai-Khentei belt into the Zag-Haraa(ZH), Asralt-hairhan (AH), Kharhorin (HH),
Tsetserleg (TT), Ulaanbaatar (UB), and Onon (ON)terranes (Fig. 2).
The Devonian-Carboniferous rocks of theUlaanbaatar terrane are subdivided into the following
four lithostratigraphic units, the Sergelen, Gorkhi,Altan-Ovoo, and Orgioch-Uul Formations (Minjinet al., 2006), with the former two are upper Paleozoic
accretionary complexes (Kurihara et al., 2009), and Fig. 2 Simplified geological map around Ulaanbaatar area
(modified from Tomurtogoo et al., 1998).
latter two are regarded as Carboniferous shallow
marine system (Minjin et al., 2006). Takeuchi et al.
(2013) newly divided the Paleozoic rocks around Ulaanbaatar into the Altan-Ovoo & Orgioch-Uul andGorkhi Formations of accretionary complexes, and the Carboniferous shallow marine system.
The Gorkhi Formation consists of sandstone, mudstone, alternating beds of sandstone and mudstone— 20 —

of turbidite affinity and chert, with small amounts of siliceous shale, basalt, limestone and clast-bearing
mudstone (Kurihara et al., 2009). The chert of the Gorkhi Formation yields Upper Silurian to Upper
Devonian radiolarians and conodonts (Kurihara et al., 2009). The Altan-Ovoo Formation consists ofsandstone, mudstone and shale, and the Orgioch-Uul Formation consists mainly of sandstone and mudstone
with conglomerate intercalations (Minjin et al., 2006). The Gorkhi Formation is thought to be in fault
contact with the Altan-Ovoo Formation (Magic Project, 1998; Minjin et al., 2006).
The study area is southeast of Ulaanbaatar, Gachuurt-Nalaikh area. The rocks in the study area havebeen assigned to the Gorkhi, Altan-Ovoo, and Orgioch-Uul Formations (e.g., Magic Project, 1998;
Tomurtogoo et al., 1998; Minjin et al., 2006).
3. Lithology and geological structure in the Gachuurt-Nalaikh area
The rocks of this area are composed mainly of thick massive sandstone, and minor bedded sandstone,
alternating beds of sandstone and mudstone, and conglomerate with chert slabs (Fig. 3). The rocks
generally strike NE to NW, steeply dip north or south, and are complexly folded in the north of the study
area (Fig. 3). The axial planes of these folds strike NE and steeply dip north or south. The rocks of thisarea cut by several NW- and NE-trending vertical faults. In the west of the study area, the rocks are in
fault contact with Mesozoic Granite.
The sandstone (Fig. 4A), greenish gray to dark gray, is commonly massive and coarse- to mediumgrained, but rarely bedded and fine-grained. The sandstone is ill-sorted, with dominantly angular to very
angular grains. A bed of the alternating beds of sandstone and mudstone, 10 to 30 cm thick, exhibit
grading and cross lamina (Fig. 4B). The mudstone is black to gray, commonly fissile but rarely massive(Fig. 4C). The conglomerate including granules to boulders of red chert and sandstone are rarely observed
at north of Nalaikh (Fig. 4D).
The chert slabs, generally several tens of meters thick, are structurally intercalated in the non-bedded
massive sandstone (Fig. 4E). The chert, red and well-bedded with muddy films, includes numerous
spherical radiolarian tests (Fig. 4F). A bed of the chert is generally 5 to 10 cm thick.
An eastward-facing conformable succession of chert, siliceous shale, mudstone and sandstone, inascending order, is exposed at north of Nalaikh (Section 20100808, N47.829790°E 107.181931°; Figs.
5 and 6). The rocks in this section strike N 10° to 40°E and dip 70° to 90° to the north. The chert is infault contact with the underlying sandstone at its western end and is conformably overlain by the siliceous
shale at its eastern end (Figs. 5 and 6A-B). The chert is folded in syncline (Fig. 6C). The axial plane of
the fold strikes NE and steeply dips north. Thickness of the chert is at least 10 m. The siliceous shale andthe mudstone are several tens of centimeters thick each other.
4. Radiolarians from the chert lens at Section 20100808
Poorly preserved radiolarian fossils were recovered by etching in dilute hydrofluoric acid for 24 hours
from a sample of red chert at Section 20100808. Individual radiolarians liberated from the matrix werewashed and sieved at 63 and 108-micron fractions. Radiolarians were picked from the dried residues andidentified with the aid of reflected light and scanning electron microscopes.
Although most radiolarians do not retain their surface structures and spines, we identified Deflantricasp., characterized by basal spines with an irregular shell (Fig. 7). This genus has previously been reported
from the Lower Devonian of Japan (e.g., Furutani, 1983; Wakamatsu et al., 1990; Kurihara and Sashida,2000).

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Fig. 3 Geological map in Gachuurt-Nalaikh area. See Fig. 1 for the location of the mapped area.

Fig. 3

Fig. 4 Lithologies in the study area. See Fig. 2 for the location. (A) Thick sandstone. (B) Alternating beds ofsandstone and mudstone with grading. Stratigraphic top is upper on the picture. (C) Mudstone. (D)Chert, red and well-bedded with muddy films. (E) Conglomerate including boulders of red chert. (F)Photomicrograph of radiolarian chert. Plane-polarized light. Scale bar = 0.5mm.

Fig. 5 Route map of section 20100808. See Fig. 2 for the location.
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Fig. 5

5.

Fig. 6 Lithologies in section 20100808. See Fig. 4 forthe location. (A) Chert in fault contact withunderlying sandstone. (B) Chert conformably
overlain by siliceous shale and sandstone. (C)Syncline in chert.

Fig. 7 Early Devonian radiolarians from section 20100808. All scale bars represent 100 μm. (1) Deflantrica sp. (2,3) spherical radiolarians.

Discussion
Geological division of the rocks at the Gachuurt-Nalaikh area
Although the rocks of this area have been previously divided into the Gorkhi, Altan-Ovoo, and OrgiochUul Formations from south to north (e.g., Magic Project, 1998; Tomurtogoo et al., 1998; Minjin et al.,2006; Fig. 3), there are no significant structural and lithological gaps across the boundaries between theseformations. In addition, the sandstones of the Gorkhi, Altan-Ovoo, and Orgioch-Uul Formations in thisarea are mostly similar and cannot be distinguished each other in their texture and grain composition(Suzuki et al., 2013). Therefore, there is no reason to divide the rocks of this area into the three formations,and they should be regarded as a single geological unit.
Several slabs of bedded radiolarian chert, ca. 1 to 3 km in length, are intercalated in the massive
sandstone in this area. Although actual boundary between the chert and the surrounding sandstone cannot
be observed due to poor exposure, the sandstone around the slabs never includes clasts or fragments ofchert, and does not show sedimentary structures such as bedding and slumping. These observations
suggest that the chert slabs were not olistostromally settled as sedimentary blocks in the sandstone.
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Furthermore, a conformable succession of chert, siliceous shale, mudstone and sandstone in ascendingorder is exposed at Section 20100808. This litho-stratigraphical set has generally been described as a partof ocean plate stratigraphy (OPS) at stacked tectonic slices of accretionary complexes through thePhanerozoic (e.g., Kamiaso Unit of the Mino belt, Southeast Japan; see Kimura and Hori, 1993, Nakae,2000). Therefore the repetition of chert and clastic rocks with OPS within this area might show thestacking of tectonic slices of the chert-clastic rock sequence within an accretionary complex.
The rocks in and around Ulaanbaatar have been previously divided into the Gorkhi Formation thatconsists mainly of stacking sheets of a chert-clastic rock sequence within an accretionary complex(Kurihara et al., 2009), and the Carboniferous shallow marine system (Orgioch-Uul and Altan-OvooFormations) that consists largely of sandstone, mudstone and conglomerate (Minjin et al., 2006). Takeuchi
et al. (2013) newly divided the Paleozoic rocks around Ulaanbaatar into the Altan-Ovoo & Orgioch-Uuland Gorkhi Formations of accretionary complexes, and the Carboniferous shallow marine system. Althoughmost of the rocks in the study area have been previously assigned to the Carboniferous shallow marinesystem (e.g., Magic Project, 1998; Tomurtogoo et al., 1998; Minjin et al., 2006), they are the stackingof tectonic slices within an accretionary complex as mentioned above. Moreover, the rocks in this area
are lithologically and stratigraphically similar to those not of the Altan-Ovoo & Orgioch-Uul Formation
but of the Gorkhi Formation.
Kurihara et al. (2009) reported Upper Silurian to Upper Devonian radiolarians and conodonts from aslab of red radiolarian chert of the Gorkhi Formation at Section 20040813B (Fig. 3), about 5 km southeastof this area. The radiolarian fossils presented here possibly suggest that the chert of this area can becorrelated with that in the Gorkhi Formation in their age.
These lithological, stratigraphical, and chronological facts suggest that the rocks of this area should
be assigned to the Gorkhi Formation. Consequently, it is appropriate that the rocks of this area are not of
the Carboniferous system but regarded as the northern extension of the Gorkhi Formation.
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. This work was supported by Grant in Aid for scientificresearch by the Ito Kagaku Shinko-kai and the Japan Society for the Promotion of Science (No. 20403013),
Grant in Aid for JSPS Fellowship (No. 02087), and the Socho-Sairyo-Keihi of the Nagoya University,
Japan.
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（2012 年 10 月 15 日受付，2012 年 12 月 25 日受理）

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