The Cenozoic rotational extrusion of the Chuan Dian Fragment: New paleomagnetic results from Paleogene red-beds on the southeastern edge of the Tibetan Plateau

    The Cenozoic rotational extrusion of the Chuan Dian Fragment: New paleomagnetic results from Paleogene red-beds on the southeastern edge of the Tibetan Plateau Ya-Bo Tong, Zhen-Yu Yang, Heng Wang, Liang Gao, Chun-Zhi An, Xu-Dong Zhang, Ying-Chao Xu PII: DOI: Reference:

S0040-1951(15)00374-1 doi: 10.1016/j.tecto.2015.07.007 TECTO 126688

To appear in:

Tectonophysics

Received date: Revised date: Accepted date:

9 June 2014 11 May 2015 13 July 2015

Please cite this article as: Tong, Ya-Bo, Yang, Zhen-Yu, Wang, Heng, Gao, Liang, An, Chun-Zhi, Zhang, Xu-Dong, Xu, Ying-Chao, The Cenozoic rotational extrusion of the Chuan Dian Fragment: New paleomagnetic results from Paleogene redbeds on the southeastern edge of the Tibetan Plateau, Tectonophysics (2015), doi: 10.1016/j.tecto.2015.07.007

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ACCEPTED MANUSCRIPT The Cenozoic rotational extrusion of the Chuan Dian Fragment: New paleomagnetic results from Paleogene

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red-beds on the southeastern edge of the Tibetan Plateau

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Institute of Geomechanics, Chinese Academy of Geological Science, Beijing 100081, China

Key laboratory of Paleomagnetism and Tectonic Reconstruction, the Ministry of Land and Resources, Beijing,

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Ya-Bo Tonga, b, Zhen-Yu Yanga, b*, Heng Wanga, Liang Gaoa, Chun-Zhi Ana, Xu-Dong Zhangc, Ying-Chao Xua

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100081, China

East China Mineral Exploration & Development Bureau For Non-Ferrous Metals, Nanjing, 210007, China

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* Corresponding author. Tel.: +86 10 88815152

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E-mail address: [email protected] (Z.Y. Yang)

Abstract: Paleomagnetic studies were conducted on the Eocene and Oligocene strata at the western part of

the Chuan Dian Fragment in order to describe the crustal deformation induced by continuous penetration of the

Indian plate into Eurasia during the late Cenozoic. High-temperature magnetic components with unblocking

temperatures of ~680°C were isolated, and positive fold and/or reversal tests reveal the primary nature of the

magnetization. The tilt-corrected site-mean directions obtained from the Oligocene and middle-early Eocene strata

are Ds = 200.9°, Is = –31.3°, k = 52.8, α95 = 7.7°; and Ds =29.7°, Is =32.0°, k =44.9, α95 = 5.6°, respectively. Comparison of these results with previous paleomagnetic data from the Chuan Dian Fragment shows that the

western and central parts of the Chuan Dian Fragment experienced ~20° integral clockwise rotation relative to East

Asia since the middle Miocene. However, the eastern part of the Chuan Dian Fragment has experienced different

rotational deformation relative to East Asia since the Pliocene, because of the intense regional crustal deformation

ACCEPTED MANUSCRIPT and activity on fault systems. The eastern boundary of the Chuan Dian Fragment was bounded by the

Yuanmou-Luezhijiang left lateral strike-slip fault prior to the Pliocene, and then substituted by the Xiaojiang left

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lateral strike-slip fault since the Pliocene, due to the eastwards spreading of the clockwise rotational movement of

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the Chuan Dian Fragment. The evolutionary characteristics of the Ailaoshan-Red River and Xianshuihe-Xiaojiang

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strike-slip faults were controlled by the difference between the clockwise rotational extrusion velocities of the

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Chuan Dian Fragment and the Indochina Block.

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Keywords: Eocene, Oligocene, Paleomagnetism, Chuan Dian Fragment.

Introduction

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The collision between the Indian plate and Eurasia during the Paleogene, and the ensuing approximate

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northward indentation of India into Asia, induced the intense crustal deformation of Eurasia (Aithchison et al.,

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2007；Beck et al., 1995; Jaeger et al., 1989; Klootwijk et al., 1985; Molnar and Tapponnier, 1975; Rowley, 1996;

Van Hinsbergen et al., 2012), and widely developed strike-slip fault systems on and around the Tibetan Plateau

(Leloup, 1995; Molnar and Dayem, 2010; Tapponnier et al., 1990; Wang et al., 1998a, 1998b; Wang and Burchfiel,

2000). Previous geological and paleomagnetic studies have demonstrated that ~1300–2500 km of northward

convergence has occurred between India and Eurasia since the Paleocene (Canda and Stegman, 2011; Cogné et al.,

2013; Copley et al., 2010; Dupont-Nivet et al., 2010; Liebke et al., 2010; Lippert et al., 2011; Ma et al., 2014;

Molnar and Stock, 2009; Sun et al., 2010; Van Hinsbergen et al., 2011; Yang et al., 2014), which may have been

accommodated by latitudinal crustal deformation and shortening in and around the Tibetan Plateau (Yin and

Harrison, 2000; Spurlin et al., 2005; Yin et al., 2007; Van Hinsbergen et al., 2011), and lateral rotational escape of

crustal materials on the southeastern and northeastern edges of the Tibetan Plateau (Akciz, 2008; Dewey et al.,

1989; Jin et al., 1996; Kornfeld et al., 2014; Otofuji et al., 2007; Replumaz and Tapponnier, 2003; Tapponnier et al.,

ACCEPTED MANUSCRIPT 1982, 2001; Tanaka et al., 2008; Tong et al., 2013; Yin and Harrison, 2000; Yin., 2010).

The Chuan Dian Fragment (CDF) is a composite of terrane that consists of the southwestern part of the South

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China Block and the southern part of the Songpan-Ganzi fold belt, which is bounded by the Jinsha-Ailaoshan-Red

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River strike-slip fault (JARF) in the west, and by the Yushu-Xianshuihe-Shimian-Xiaojiang left lateral strike-slip

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faults (YSF-XSHF-SMF-XJF) in the east (Wang et al.,1998b, 2014) (Fig. 1A). The current southeastern edge of

the Tibetan Plateau comprises the Shan Thai Block (STB), the Indochina Block (ICB) and the CDF (Fig. 1A). The

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STB and ICB are situated on the southern side of the JARF. The Gaoligong right lateral strike-slip faults (GLGF)

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and Sagaing right lateral strike-slip faults (SGF) constitute the western boundary of the STB, and the Chongshan

strike-slip fault (CSF) and Lancangjiang suture zone (LCJSZ) constitute the eastern boundary. The ICB is located

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between the JARF and CSF-LCJZ. Previous paleomagnetic studies of the Cretaceous and Paleogene rocks are

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spread across the STB and ICB (Funahara et al., 1992, 1993; Huang and Opdyke, 1993; Otofuji et al., 2012; Sato

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et al., 1999, 2001, 2007; Tanaka et al., 2008; Tong et al., 2013; Yang et al., 1993, 2001a, 2001b). Statistical

analysis of this paleomagnetic dataset indicate that the STB and ICB have experienced ~20º–35º integral clockwise

rotation, accompanied by ~500 km southeastwards extrusion along the JARF and GLGF-SGF, relative to the South

China Block (SCB) since the Oligocene (Tanaka et al., 2008; Tong et al., 2013; Yang et al., 1995). A GPS dataset

for areas internal to and surrounding the Tibetan Plateau further confirms that the crustal materials have

experienced clockwise rotations around the Eastern Himalaya syntaxis (Fig. 1) (Chen et al., 2000; Gan et al., 2007;

Shen et al., 2005). Such crustal deformation is thought to be the result of ductility in upper-crustal materials that

are escaping southeastwards, driven by viscous lower-crustal flow channels (Clark and Royden, 2000; Royden et

al., 1997, 2008). Based on field observations of late Cenozoic fault systems and geomorphology of the

southeastern edge of the Tibetan Plateau, Wang et al. (1997, 1998b, 2014) also suggested that the CDF and the

northwestern part of ICB have been rotated along a fault system of the XSHF-SMF-XJF and Dien Bien Phu

ACCEPTED MANUSCRIPT strike-slip fault (DBPF) since the Pliocene.

The available Cretaceous and Paleogene paleomagnetic data from the CDF have been obtained mainly from the

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eastern and middle part of the CDF (Fig. 1B), and indicate that the central part of the CDF experienced ~20º

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integral clockwise rotation, and that the eastern part of the CDF experienced a clearly different rotation in the

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Cenozoic (Funahara et al., 1992; Huang and Opdyke, 1992; Otofuji et al., 1998; Tamai et al., 2004; Yang et al.,

2001a; Yoshioka et al., 2003). However, paleomagnetic data from the western part of the CDF are scarce, which

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limits our understanding of the rotational deformation process of the CDF in the southeastern edge of the Tibetan

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Plateau during the late Cenozoic. Thus, the goal of the present study is to obtain paleomagnetic data from

Oligocene and Eocene red-beds of the western part of the CDF in order to reveal the rotational extrusion

Regional geology and sampling

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characteristics and the tectonic evolution of the CDF.

The study area is located in the northwestern part of the CDF, which belongs to the Songpan-Ganzi fold belt.

The crustal basement mainly comprises of Paleozoic strata overlain by Permian-Triassic neritic- and bathyal-facies

limestone formations. The Paleozoic and Triassic strata were both influenced by tectonism of the Indosinian

orogeny, which formed a widespread linear fold system of closely spaced NW-SE-trending folds. The

Eocene-Oligocene red-beds are mainly distributed in the western side of the Jianchuan-Lijiang left lateral

strike-slip fault in the Jianchuan area of the western part of the CDF, which unconformably overlies the Mesozoic

marine-facies limestones. The strata have experienced crustal deformation, inducing a fold system in the Paleogene

strata with NW-SE trending fold axes (BGMRY, 1990; Yang et al., 2014).

Our paleomagnetic sampling sections are located in the Jianchuan area, where the Eocene strata mainly

comprise the late Eocene Baoxiangsi Formation and the early–middle Eocene Guolang Formation. The Baoxiangsi

ACCEPTED MANUSCRIPT Formation (total thickness of ~800 m) consists of medium-grained gray and purple-red coarse sandstone, which

was not sampled in the present study. The early-middle Eocene Guolang Formation conformably underlies the

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Baoxiangsi Formation, which consists mainly of purple-red siltstone, mudstone, gray calcareous siltstone, and

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sandstone with a total thickness of ~1620 m. Fossil assemblages with abundant ostracods (e.g., Cypridea

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xindianensis, Cyprinotus cf. lectus, Ilyocypris dunshanensis), gastropods (e.g., Grandipatula parva, Assiminea

retopercula, Radix subbullata, Cochlicopa cf. headonensis), and conchostracans (e.g., Paraleptestheria

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menglaensis, P. yunlongensis) in the Guolang Formation indicate an early–middle Eocene age (BGMRY, 1990). A

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total of 262 core samples from 21 sites were obtained from the early–middle Eocene Guolang Formation in the

southwest and north sections of the Jianchuan area, seven sites (JL1-JL7) were sampled along the provincial road

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from Madeng to Jianchuan town, and 14 sites (JL8-JL21) were sampled in Laojun Mountain (Fig. 2A, B, C).

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The Oligocene Jinsichang Formation unconformably overlies the late Eocene Baoxiangsi Formation with a

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thickness of ~1700 m (BGMRY, 1990). The upper part of the Jinsichang Formation consists of gray conglomerate

and gray–khaki sandstone, while the lower part consists of purple-red siltstone, red fine sandstone and gray

sandstone. A total of 184 core samples from 14 sites were obtained from the lower part of the Oligocene Jinsichang

Formation (SJ1-SJ14) in the Jinchuan area (Fig. 2A, D).

All paleomagnetic samples were collected using a portable drill and oriented with a magnetic compass. The

location of each sampling site was determined using a portable GPS. The present-day geomagnetic direction at

each sampling locality was calculated from the International Geomagnetic Reference Field (2010) (International

Association of Geomagnetism and Aeronomy, Working Group V-MOD, 2010).

3.

Rock magnetism

The progressive acquisition of isothermal remanent magnetization (IRM) can be used to reveal the coercivity

ACCEPTED MANUSCRIPT spectrum of magnetic minerals, while the unblocking temperatures of different magnetic minerals can be revealed

by thermal demagnetization of a three-component IRM (imparted successively to each of the three axes using

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different DC fields: 2.4 T for the Z axis, 0.4 T for the X axis, and 0.12 T for the Y axis) (Lowrie, 1990). Based on

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the distribution of the paleomagnetic sites and the lithological characteristics of the samples, eight specimens were

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selected from the Oligocene and Eocene sampling sections for rock magnetic experiments: SJ1-7, SJ5-3, SJ10-11

early–middle Eocene Guolang Formation (Fig. 3).

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and SJ14-8 from the Oligocene Jinsichang Formation, and JL6-11, JL10-7, JL16-8 and JL20-1 from the

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The results demonstrate almost identical magnetic behavior of each of the eight red-bed specimens from the

Oligocene Jinsichang Formation and the early–middle Eocene Guolang Formation. Thermal demagnetization of a

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three-component IRM of the eight specimens shows that the hard and medium components were reduced abruptly

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when the demagnetization temperature reached 620°C–650°C, with unblocking occurring at ~680°C, indicating the

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presence of abundant hematite (Fig. 3A-a, 3B-a). The hard, medium and soft components also exhibit slight

inflections when the demagnetization temperature reached ~560°C–580°C, indicating the presence of magnetite

(Fig. 3A-a,3B-a). The IRM acquisition curves show that the magnetic remanence approached saturation when the

applied DC field approached 2400 mT (Fig. 3A-b, 3B-b). The magnetic remanence decreased rapidly and became

negative when reversed fields of 400–700 mT were applied, indicating that the magnetic minerals have a high

coercivity (Fig. 3A-b, 3B-b). Therefore, we conclude that abundant hematite and minor magnetite are the main

magnetic carriers in the Oligocene Jinsichang Formation and the early-middle Eocene Guolang Formation.

4.

Paleomagnetic results

All core samples were cut into a length of 2.2–2.3 cm in the laboratory. Specimens were subjected to stepwise

thermal demagnetization using an ASC TD-48 thermal demagnetizer, and remanent magnetization was measured

ACCEPTED MANUSCRIPT using a 2G-755 cryogenic magnetometer. All paleomagnetic experiments were conducted at the Key Laboratory of

Paleomagnetism and Tectonic Reconstruction, Ministry of Land and Resources in Beijing. Stepwise thermal

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demagnetization was performed up to 695°C. The temperature interval of thermal demagnetization was 50–100°C

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initially, and 10–20°C at higher temperatures. The magnetic behavior of the specimens during demagnetization

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was plotted on a Zijderveld diagram (Zijderveld, 1967; Cogné, 2003), and analyzed using principal component

analysis (Kirschvink, 1980) or the best-fit great circles method (McFadden and McElhinny, 1988). Site-mean

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directions were calculated using Fisher statistics (Fisher, 1953) and/or the intersection of great circles (McFadden

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and McElhinny, 1988).

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4.1 Paleomagnetic results for the Jinsichang Formation

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The samples from the Oligocene Jinsichang Formation can be divided into three types based on their thermal

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demagnetization characteristics: (i) The first type consists of specimens from sites SJ2, SJ3, SJ6, SJ9 and SJ12,

with a lithology consisting mainly of gray-brown sandstone and sandstone containing quartz veins. The thermal

demagnetization behaviors are unstable, and therefore the magnetic components cannot be isolated. (ii) The second

type consists of specimens from sites SJ1, SJ2 and SJ14. The direction of the magnetic component vector did not

converge to the origin when the thermal demagnetization temperature exceeded 600°C, and thus the

high-temperature magnetic component cannot be isolated using principal component analysis (Kirschvink, 1980)

(Fig. 4A-a). However, the demagnetized directions changed along the great circles, indicating that the directions of

characteristic magnetic components are concealed. The site-mean direction of the high-temperature components of

these sites was determined using the intersection of great circles method (McFadden and McElhinny, 1988) (Fig.

4A-a). (iii) The third type consists of specimens from sites SJ5, SJ7, SJ8, SJ10, SJ11 and SJ13. Here, the

high-temperature magnetic components converged linearly towards the origin and were isolated between 400°C

ACCEPTED MANUSCRIPT and 680°C (Fig. 4A-b).

The viscous remanence of a low-temperature magnetic component was isolated from 31 specimens at seven

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sites when the thermal demagnetization temperature reached ~200–300°C. The sample-mean direction of the

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formation is Dg = 349.4°, Ig = 33.2°, kg = 46.3, α95 = 3.8° (n = 31 samples) before tilt correction, which is close to

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that of Earth’s magnetic field (D = 358.6°, I = 31.0°), and Ds = 352.0°, Is = 19.6°, ks = 18.4, α95 = 6.2° after tilt correction (Fig. 5A). The precision parameter (k) decreased from 46.3 (kg) to 18.4 (ks) during unfolding,

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suggesting that the low-temperature component is a recently-acquired viscous remanent magnetization.

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The high-temperature magnetic components were isolated from nine sites of the Oligocene Jinsichang

Formation, amongst which seven sites show reversed polarity and the other two sites show normal polarity (Table

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1). Because of the large uncertainty for site SJ4 (α95=72.2°), the data were excluded from the statistical analysis.

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The site-mean direction is Dg = 213.6°, Ig = –46.5°, kg =22.8, α95 = 11.9° (N = 8 sites) before tilt correction, and

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Ds = 200.9°, Is = –31.3°, ks =52.8, α95 = 7.7° after tilt correction (Fig. 6A). Although the precision parameters increase significantly after tilt correction (ks/kg = 2.31 < F (14, 14) = 2.48), the fold test is inconclusive at the 95%

confidence level according to the fold test methods of McElhinny (1964) and McFadden (1990) (The calculated

values were ξ1(in situ) = 0.59 in geographic coordinates and ξ1(tilt corrected) = 0.55 after tilt correction, while the critical value at the 95% confidence level is ξC =3.29). The inconclusive fold test may be related to the approximately uniform northward dip of the sampling strata, with only one sampling site (SJ14) dipping towards the southeast

(Fig. 2D). Although the parameter (k) reaches a maximum (kmax = 57.0) at 80.8% during progressive unfolding,

the direction (Dmax= 202.5°, Imax= –34.6°) is very similar to the mean direction after tilt correction (Fig. 6A).

The fold test is positive according to the method of Watson and Enkin (1993) (with DCslop = 0.83±0.49). The reversal test is positive at the 95% confidence level (R = 0.14, Critical R value at 95% = 0.65; average Gamma =

12.4 < Critical Gamma = 16.9) (McFadden and Lower 1981; McFadden and McElhinny, 1990). Thus, the

ACCEPTED MANUSCRIPT reliability test indicates that the remanent magnetization of the high-temperature magnetic components is

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characteristic of a pre-fold origin.

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4.2 Paleomagnetic results for the Guolang Formation

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The magnetic behavior of specimens from the early–middle Eocene Guolang Formation can also be divided

into three types based on their thermal demagnetization characteristics: (i) The first type consists of specimens

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from sites JL9, Jl11, JL13 and JL15, consisting of coarse gray sandstone and quartz sandstone. The thermal

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demagnetization curves are erratic, and the magnetic component cannot be isolated. (ii) The second type consists

of specimens from sites JL5, JL10, and JL14. The directions of the magnetic component vector did not trend

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towards the origin when the thermal demagnetization temperature exceeded 600°C, however, they changed along

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great circles on the equal-area projections. The intersection of great circles method was used to calculate the mean

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direction of the high-temperature magnetic component (McFadden and McElhinny, 1988) (Fig. 4B-a). (iii) The

thermal demagnetization results of the third type demonstrate the presence of linear high-temperature magnetic

components between 400 °C and 680 °C that converge towards the origin (Fig. 4B-b).

Low-temperature components were isolated from 38 specimens at nine sites when the thermal

demagnetization temperature reached 200–300°C. The sample-mean direction is Dg = 356.8°, Ig = 29.7°, kg =

31.8, α95 = 4.2° (n = 38 samples) before tilt correction, and Ds = 357.9°, Is = 28.8°, ks = 30.1, α95 = 5.1° after tilt correction (Fig. 5B). The precision parameter (k) decreased slightly and the α95 value increased slightly after tilt correction. The formation mean direction before tilt correction is close to that of the Earth’s magnetic field in the

sampling area (D = 358.6°，I = 31.0°), indicating that the low-temperature component may represent a recent

viscous remanent magnetization.

The high-temperature component was isolated from 17 sites in the early–middle Eocene Guolang Formation,

ACCEPTED MANUSCRIPT with nine sites of normal polarity and the other eight sites of reversed polarity (Table 2). Because of the large α95 value for site JL7 (18.5°), the data were excluded from further consideration. The site-mean direction is Dg = 28.8°,

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Ig = 35.0°, kg = 22.9, α95 = 7.9° (N = 16 sites) before tilt correction, and Ds = 29.7°, Is = 32.0°, ks = 44.9 α95 = 5.6°

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after tilt correction (Fig. 6B). The bedding attitudes of most of the sampled strata of the Eocene Guolang

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Formation are gentle with very low dip angles, which may lead to a variable strike direction (Fig. 2B, C). The fold

test is positive at the 95% confidence level according to the method of McElhinny (1964) (ks/kg =1.96> F (30, 30)

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= 1.84), and/or the method of Watson and Enkin (1993) (DCslope= 1.3±0.39). The reversal test (McFadden and

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Lower 1981; McFadden and McElhinny, 1990) is positive at the 95% confidence level with statistical parameters R

= 0.12, Critical R at 95% = 0.24, and average Gamma = 7.8 < Critical Gamma = 10.9. These results indicate that

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5. Discussion

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the remanence of the high-temperature component recorded in the Eocene strata was of pre-fold origin.

The characteristic magnetic components were isolated from the early–middle Eocene Guolang Formation and

the Oligocene Jinsichang Formation in the Jianchuan area of the western part of the CDF. The positive fold test

confirmed a pre-folding origin for these paleomagnetic data. The Eocene-Oligocene strata were probably folded

twice in the Jianchuan area, indicated by the unconformities between the Oligocene and Eocene strata, and

between the Miocene and Oligocene strata in the western part of the CDF (BGMRY, 1990). The folding of the

Eocene and Oligocene strata probably occurred prior to the Oligocene and Miocene, respectively. The

characteristic remanence obtained from the early-middle Eocene Guolang Formation and the Oligocene Jinsichang

Formation is therefore of pre-Miocene origin. Furthermore, the directions of high-temperature components isolated

from all three sampled sections are of both normal and reversed polarity, which pass the reversal test at the 95%

confidence level. Thus, the results indicate that the characteristic magnetic components are the primary

ACCEPTED MANUSCRIPT remanences that were acquired at the time of rock formation.

A plunging fold may induce the deviation of the declination of paleomagnetic data, however, it was difficult to

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judge in the field whether or not the paleomagnetic sampling sections suffered from this problem. In general, a fold

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with an intensely plunging fold axis would cause the declination to increase in one fold limb and to decrease in

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another limb. Thus the equal-area projection of the high-temperature components of samples obtained from the

two limbs of the fold would exhibit a clear elongation in the latitudinal direction, indicating that the declination

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was affected by the plunging fold axis. Figure 6 shows there is no obvious elongation in the latitudinal direction

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for the paleomagnetic data from the Jianchan area, and furthermore, the dip of the sampled strata is relatively low,

indicating only the minor influence of a plunging fold axis.

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In order to reveal the Cenozoic rotational deformation characteristics and tectonic evolution of the CDF, we

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selected and compared all of the reliable Cretaceous and Cenozoic paleomagnetic data from the CDF. Most of the

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Cretaceous and Paleogene data were selected from the eastern part of the CDF, and the Pliocene data were from

the Dali and Yuanmou areas in the central and eastern parts of the CDF. Below, all of the data from the CDF are

compared with reference paleopoles from East Asia.

5.1 Reference paleopoles for comparison

Selecting coeval paleopoles from stable crustal blocks as reference is essential for evaluating the deformation

process of the studied areas. The Cretaceous and Cenozoic paleopoles of the SCB and Eurasia have often been

selected as reference paleopoles for crustal deformation studies of East Asia (Funahara et al., 1992, 1993; Huang

and Opdyke, 1993; Otofuji et al., 2012；Sato et al., 1999, 2001, 2007; Tanaka et al., 2008; Tong et al., 2013; Yang

et al., 1993, 1995, 2001a, 2001b). Recently, instead of using data transferred from Western Europe, Cogné et al.,

(2013) chose a set of Cenozoic paleopoles obtained from East Asia and constructed a new Apparent Polar

ACCEPTED MANUSCRIPT Wandering Path (APWP) for East Asia, which may provide more precise interpretations of the Asian Cenozoic

deformation pattern related to the India-Eurasia collision. We divided the Cenozoic paleopoles for East Asia

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(Cogné et al, 2013) into several groups according to the geological timescale (2013), and then calculated the

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average paleopole for each geological time interval from the Cretaceous to the Pliocene (Table. 3). The average

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paleopoles were selected as reference paleopoles to estimate the rotations and latitudinal displacements of the CDF

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relative to the stable area of East Asia (Table. 4).

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5.2 Inclination shallowing of Cenozoic red-beds and latitudinal displacement of the CDF

It has been proposed that inclination deviation in eastern Asia might be the result of depositional and/or

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compaction-induced inclination shallowing in hematite-bearing red-beds (Garces et al., 1996; Tan et al., 1996;

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Wang and Yang, 2007). Previous Cretaceous paleomagnetic data from the southern side of the JARF show that

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since the Paleogene the STB and ICB have undergone ~600–1000 km of southeastward extrusion along the JARF

and GLGF-SGF (Sato et al, 1999, 2001, 2007; Tanaka et al., 2008; Yang et al., 2001a, 2001b; Yang and Besse,

1993; Zhang et al., 2012). Recently, based on the elongation/inclination (E/I) correction method (Tauxe and Kent,

2004), Tong et al. (2013) suggested that the magnetic inclination of Eocene strata from the northwestern part of the

CDF may have suffered a ~10º shallowing. After correction for inclination shallowing, the Eocene inclination is

similar to that of the Cretaceous, implying an almost constant paleolatitude during the Cretaceous and Eocene.

The Pliocene paleomagnetic data of the Yuanmou area and Paleocene paleomagnetic data of the Huidong

area indicate that the CDF may have experienced ~10° northward displacement relative to the stable area of East

Asia (Table. 4, Fig. 7A) (Huang and Opdyke, 1992; Li et al., 2013; Zhu et al., 2008). However, the Paleogene and

Cretaceous paleomagnetic data obtained in other studies show less than 5.3° ± 4.5° northward displacement of the

CDF (Funahara et al., 1992; Huang and Opdyke, 1992; Tamai et al., 2004; Yang et al., 2001a; Yoshioka et al., 2003)

ACCEPTED MANUSCRIPT or even smaller southward displacement (Huang and Opdyke, 1992; Otofuji et al., 1998) (Table 4, Fig. 7A).

However, inclination shallowing tests were not conducted on these data in the CDF. In order to test whether

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inclination shallowing existed in the hematite-bearing red-beds in the CDF, we used the elongation/inclination (E/I)

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correction method (Tauxe and Kent, 2004) to test the paleomagnetic data from the Oligocene Jinsichang Formation

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and the early–middle Eocene Guolang Formation in the Jiangchuan area. The E/I result for the Oligocene data

yielded a corrected inclination of 33.9°, with an error range of 28.3° to 43.2° (Fig. 8); in addition, the early-middle

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Eocene data yielded a corrected inclination of 37.9°, with an error range of 31.2° to 44.9° (Fig.8). The corrected

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inclinations are all slightly greater than the measured inclinations (Table. 4), indicating that the CDF did not

experience an obvious latitudinal displacement since the Eocene (Fig.7A).

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A limited amount of latitudinal displacement of the CDF is in accordance with geological results which

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indicate that the CDF was extruded southward at least ~60 km along its northeastern boundary with the left lateral

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strike-slip fault system of XSHF-SMF-XJF since ~17–12 Ma (Roger et al., 1995; Wang et al., 1998b; Wang et al.,

2008, 2009, 2012; Zhang et al., 2004). The results are supported by GPS measurements of the internal and

surrounding area of the Tibetan Plateau which indicate that crustal materials currently experience clockwise

rotational movement around the Eastern Himalaya Syntaxis (Chen et al., 2000; Gan et al., 2007；Shen et al., 2005).

5.3

Rotational deformation of the CDF since the late Cenozoic

The Eocene and Oligocene paleomagnetic data from the Jianchuan area in the western part of the CDF show

25.4° ± 9.1° and 18.7° ± 7.1° of clockwise rotational movement since the Oligocene, respectively, relative to East

Asia (Table. 4, Fig. 7B). Previous paleomagnetic data from the central part of the CDF indicate that the Dayao and

Zhupeng areas have experienced 21.0° ± 4.7° and 20.6° ± 3.9° of clockwise rotation, respectively, relative to East

Asia (Otofuji et al., 1998; Yang et al., 2001a) (Table. 4, Fig. 7B). However, this seems to contradict the estimations

ACCEPTED MANUSCRIPT of Yoshioka et al (2003) that the Dayao and Yongren areas have experienced 11.8° ± 4.4° and 12.4° ± 4.7° of

clockwise rotations since the Paleogene, respectively (Table 4, Fig. 7B). Careful reanalysis of the paleomagnetic

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dataset of Yoshioka et al. (2003) shows that the site-mean declinations of most of the sampling sites in the Yongren

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and Dayao areas accord with those reported by Otofuji et al. (1998) and Yang et al. (2001a) for the adjacent area,

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except for three sites (YR30: Ds = 1.5°, YR38: Ds = 13.6°, and YR40: Ds = 8.1°) displayed obvious inconsistency.

The possibility that local tectonic deformation, or the indistinct bedding attitudes of these sites, was responsible for

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the declination deviation cannot be excluded. Therefore we tried to removing three outlying data of Yoshioka et al.

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(2003), and the remaining seven sites gave a formation mean direction of Ds = 21.1°, Is = 31.4°, α95 = 5.3° for the Dayao area, which passes the McFadden fold test (McFadden, 1990) at the 95% confidence level (ξ1(in situ) = 6.90 in

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geographic coordinates and ξ1(tilt corrected) = 1.84 after tilt correction; the critical value ξC = 3.09). The result indicates

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that a 16.4° ± 4.6° clockwise rotation of the Dayao area occurred relative to East Asia (Fig. 4, Fig. 7B). The similar

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situation is found for the paleomagnetic results from Yongren area (Yoshioka et al., 2003). When the results from

four sites (YR20: Ds = 7.8°，YR27: Ds = 6.2°, YR28: Ds = 0.0°; YR29: Ds = 1.2°) were discarded, the mean

direction of the remaining twelve sites was Ds = 22.6°, Is = 26.6°, α95 = 5.8° for the Yongren area, which yields a positive McFadden fold test (McFadden, 1990) at the 95% confidence level (ξ1(in coordinates,

situ)

= 6.29 in geographic

ξ1(tilt corrected) = 1.31 after tilt correction; the critical value ξC = 4.04). The result demonstrates that the

Yongren area experienced 17.9° ± 4.7° of clockwise rotation relative to East Asia (Fig.4, Fig. 7B). Thus, the

recalculated clockwise rotations at the Dayao and Yongren areas are approximately consistent with those estimated

by Otofuji et al (1998) and Yang et al (2001a) (Fig. 7B). Combining the paleomagnetic data from the western and

central parts of the CDF, it can be estimated that the areas on the western side of the Yuanmou-Luezhijiang Fault

(YLF) have experienced ~15−20° of integral clockwise rotation as a whole since the Oligocene (Fig. 9).

On the eastern side of the YLF of the CDF, several approximately N–S-trending left lateral strike-slip faults are

ACCEPTED MANUSCRIPT developed, including the YLF, the Yimen Fault (YMF), the Puduhe Fault (PDHF), and the Xiaojiang Fault (XJF),

from west to east (Fig. 9). In addition, pronounced NE–SW-trending thrusting right lateral strike-slip faults are

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developed between these N–S-trending left lateral strike-slip faults (Fig.9). These faults cut the eastern part of the

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CDF into numerous crustal segments. The Cretaceous paleomagnetic data show ~7° of counterclockwise rotations

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for the Xichang area (Lower Cretaceous: −7.3° ± 4.4°; Upper Cretaceous: −6.7° ± 3.8°) relative to East Asia

(Tamai et al., 2004) (Table 4, Fig. 7B). However, the Late Cretaceous paleomagnetic data indicate 12.0° ± 2.9° of

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clockwise rotation for the Huili area on the southern side of Xichang (Huang and Opdyke, 1992) (Table 4, Fig. 7B).

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The Late Cretaceous and Paleocene paleomagnetic data of the Huidong area adjacent to Huili show 2.7° ± 5.0° and

6.0° ± 7.2° of counterclockwise rotation, respectively (Huang and Opdyke, 1992) (Table 4, Fig. 7B). The

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Paleocene paleomagnetic data for the Bailu area indicate ~25.9° ± 8.3° clockwise rotation relative to East Asia

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(Otofuji et al., 1998) (Table 4, Fig. 7B). The Chuxiong area is located on the southern edge of the western part of

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the CDF, and the Cretaceous paleomagnetic data yielded in this area grossly indicate 34.7° ± 8.3° clockwise

rotational movement relative to East Asia (Funahara et al. 1992) (Table 4, Fig. 7B). The diversity of paleomagnetic

data from the eastern part and the southern edge of the CDF indicates that these areas experienced a complex

pattern of different rotational movement relative to East Asia during the Cenozoic that was related to intense

regional crustal deformation and activity of fault systems developed between the YLF and XJF (Fig. 9).

Recentl paleomagnetic data from Pliocene lacustrine-facies sediments of the Yuanmou Basin on the western

side of the YLF in the central part of the CDF, indicate that the Yuanmou Basin has experienced 2.6° ± 6.5° of

clockwise rotation relative to East Asia since the Pliocene (Table 4, Fig. 7B) (Zhu et al., 2008). In addition, late

Miocene to early Pleistocene paleomagnetic data obtained from lacustrine-facies sediments in the Eryuan Basin

adjacent to the Dali area indicate that the Eryuan area experienced 4.7° ± 6.3° of clockwise rotation relative to East

Asia from the late Miocene to early Pleistocene (Table 4, Fig. 7B) (Li et al., 2013). These results indicate that the

ACCEPTED MANUSCRIPT CDF has experienced no more than ~5° of integral clockwise rotation relative to East Asia since the Pliocene,

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which is considered to be within the level of uncertainty of the paleomagnetic data.

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5.4 Tectonic evolution of the CDF since the Oligocene

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Paleomagnetic analysis shows that the YLF, dividing the CDF into western-middle and eastern parts, was an

important left lateral strike-slip fault during the tectonic evolution of the CDF. The YLF consists mainly of two

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continuous NS-striking segments, on satellite images the northern segment extends linearly and its total length is

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~300 km long. Earthquake focal mechanisms indicate that the northern segment of the YLF is an active left-lateral

fault (Liu et al., 1986). The southern segment extends ~75 km and ends at the JARF (Wang et al., 1998b). Because

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the Yuanmou Basin was a rifted basin and was controlled by the left-lateral slip movement on the YLF prior to the

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Pliocene, it contains a sequence of fine-grained lacustrine and fluvial deposits that are more than 850 m thick

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(BGMRY, 1990). Magnetostratigraphic results from the middle and upper parts (with a thickness of ~650 m) of a

sedimentary sequence in the Yuanmou Basin constrain the age of the sediments to the early Pliocene through

Pleistocene (Zhu et al., 2008). The lower part of the sedimentary sequence of the Yuanmou Basin (with a thickness

of ~200 m) was probably deposited prior to the Pliocene, indicating that the initial strike-slip shearing of the YLF

and the formation of Yuanmou Basin commenced prior to the Pliocene. Although all geological studies suggest that

the YLF was originally a left lateral strike-slip fault, and that the initial left-lateral slip movement began prior to

the Pliocene, the field evidence for strike-slip movement on the YLF is poor and only ~100–200 m of left-lateral

stream offset can be found along the YLF (Wang et al., 1998b). It is likely that the YLF was active prior to the

Pliocene, but the left-lateral movement prior to the Pliocene was stronger than that since the Pliocene. Recent

zircon U-Pb data from the northern and southern parts of the Mianning-Dechang Syenites along the northern

segment of the YLF gave concordant ages of 12-27 Ma and 11-12 Ma, respectively. This suggests that the

ACCEPTED MANUSCRIPT strike-slip shear along the northern segment of the YLF was approximately coeval with that of the XSHF (Liu et al.,

2014), and that this movement started earlier than the activity of the XJF (Fig. 10A). Since the Pliocene, the

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Yuanmou Basin has probably changed to a transpressional basin environment, and the YLF during this time has

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been a compressional fault.

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The Cretaceous and Paleogene paleomagnetic data show that the western and central parts of the CDF on the

western side of the YLF experienced ~15°–20° integral clockwise rotation relative to East Asia since the Oligocene.

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The initial eastern boundary of the CDF, involving clockwise rotational movement, was limited on the western side

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of YLF during the Miocene (Fig. 10A). Subsequently, following rotational movement of crustal material spreading

eastwards, rotational deformation was successively propagated in the area between the YLF and the

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NNHF-ZMHF-XJF. Since the Pliocene, the NNHF-ZMHF-XJF was formed and gradually became the new eastern

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boundary of the CDF (Fig. 10A). The left lateral strike-slip movement of the YLF gradually became inactive, so

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that only ~100–200 m of left-lateral displacement can be found along the YLF based on field observations (Wang

et al., 1998b). Because the XSHF and the YLF were the block boundary of the CDF prior to the Pliocene, and the

CDF experienced integral clockwise rotation, the total left-lateral displacement of the YLF should be similar to

that of the XSHF during the interval of the middle Miocene to the Pliocene. After the middle Pliocene, the

rotational movement spread continuously eastwards, which induced the initial strike-slip movement on the SMF,

and finally the SMF gradually replaced the NNHF-ZMHF, and became the northeastern boundary of the CDF (Fig.

10A), which was evidenced by the interpretation of aerophotographs and field investigations (He et al., 2008).

On the basis of the timing of initial strike-slip movement on fault systems in the areas surrounding the Tibetan

Plateau, together with the Cenozoic rotational deformation characteristics of the CDF, STB and ICB (Li et al.,

2012; Tanaka et al., 2008; Tong et al., 2013), we suggest that the evolution of the faulting systems of the JARF and

XSHF-SMF-XJF has been controlled by the difference in the rotational extrusion velocities between the CDF and

ACCEPTED MANUSCRIPT ICB since the Oligocene. During the period from 32 Ma to 17–12 Ma, because the ICB was much closer to the

Eastern Himalaya Syntaxis than the CDF, the ICB should have been deformed earlier than the CDF by the

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approximately northward penetration of the Indian plate into Eurasia. This would have resulted in ~20° rotational

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extrusion of the ICB relative to the South China Block along the JARF in the interval from the Oligocene to the

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early Miocene (Cao et al., 2011; Leloup et al., 1995, 2001; Gilley et al., 2003; Morley, 2002; Tong et al., 2013),

whereas the CDF remained relatively stable (Fig. 10B). Left lateral strike-slip movement on the XSH-SMF-XJF

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may not yet have commenced during this period (Wang et al., 2009, 2012). Following further northward

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penetration of the Indian plate into Eurasia, the crustal deformation on the southeastern edge of the Tibetan Plateau

gradually spread northward and began affecting the CDF during the period of 17–5Ma. The initial left-lateral

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shearing of the XSHF started at ~17–12 Ma (Roger et al., 1995; Zhang et al., 2004; Wang et al., 2009, 2012),

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which induced the southeastward extrusion of the CDF. During the period of ~17–5Ma, the CDF experienced ~15°

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clockwise rotational extrusion relative to East Asia, and subsequently since ~5Ma the CDF experienced further

(~5°) clockwise rotational extrusion. In total the CDF experienced ~20° clockwise rotational extrusion relative to

East Asia since 17/15 Ma. In contrast, the STB and the northwestern part of the ICB experienced ~15° clockwise

rotational extrusion movement since ~15 Ma (Tong et al., 2013). The JARF remained relatively inactive during the

period of ~15–5 Ma (Leloup et al., 1995，2001; Gilley et al., 2003), indicating that the rotational extrusion velocity

of the STB and the northwestern part of the ICB was probably similar to that of the CDF during this period (Fig.

10B). Thus, after ca. 5Ma, the rotational extrusion velocity of the CDF gradually exceeded that of the STB and the

northwestern part of the ICB, which induced slow right lateral strike-slip movement on the JARF (Fig. 10B) (Allen

et al., 1984; Replumaz et al., 2001; Schoenbohm et al., 2006; Wang, 1998b).

6. Conclusions

ACCEPTED MANUSCRIPT (1) Paleomagnetic data from the western part of the CDF indicate that the area on the western side of the YLF

has experienced ~15–20° integral clockwise rotation relative to East Asia since the middle Miocene, and that the

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eastern side of the YLF has experienced different rotational deformation movement relative to East Asia since the

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Pliocene. The rotational movements occurred as a result of the intense regional crustal deformation and activity of

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fault systems developed between the YLF and XJF.

(2) The YLF, which divides the CDF into western and eastern parts, was formerly a left lateral strike-slip fault

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that played an important role in the tectonic evolution of the CDF. Originally, the part of the CDF that experienced

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clockwise rotational movement was limited to the area on the western side of the YLF, and prior to the Pliocene it

is likely that the YSF-XSHF-YLF constituted the northern and eastern boundary of the CDF. Subsequently,

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following the eastward spread of rotational movement, the area between the SMF and XJF was successively

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boundary of the CDF.

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incorporated into the CDF, and beginning in the Pliocene, the XJF replaced the YLF and became the new eastern

(3) The evolution of the JARF and the XSHF-SMF-XJF should be controlled by the clockwise rotational

extrusion of the CDF and ICB. During the period 32–17 Ma，the STB and ICB experienced ~20° rotational

extrusion movement because of the intense northward penetration of India into Eurasia; however, the CDF

remained relatively stable and did not begin rotational extrusion movement during this period. The JARF

experienced left lateral strike-slip movement during the period 32–17 Ma. Later, during the period 17–5 Ma,

southeastward rotational extrusion movements of the CDF initiated movement on the XSHF. The rotational

extrusion velocity of the CDF was probably similar to that of the STB and the northwestern part of the ICB, which

induced the inactivity on the JARF and intense left lateral strike-slip movement on the XSHF. After 5 Ma, the

rotational extrusion of the CDF induced left lateral strike-slip movement on the XJF and right lateral strike-slip

movement on the JARF.

ACCEPTED MANUSCRIPT

Acknowledgements

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We thank Dr. Y. Otofuji and two anonymous reviewers for their constructive reviews of the manuscript. This

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work was supported by the “National Natural Science Foundation of China (Grant 41202162)”, the “China

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Chinese Academy of Geological Sciences (Grant YWF201413).

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Geological Survey (Grant 1212011120164 and 12120114002301)” and the “Fundamental Research Funds for the

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Figure captions:

Figure 1. (A) Schematic tectonic map of the Tibetan Plateau and surrounding area. (B) Structural sketch map of

the CDF. JARF: Jinshajiang-Ailaoshan-Red River Fault; YLF; Yuanmou-Luezhijiang Fault; YMF: Yimen Fault;

ZMHF: Zemuhe Fault; XJF: Xiaojiang Fault. SMF: Shimian Fault; NNHF: Anninghe Fault; ZDF: Zhongdian Fault;

JCF: Jianchuan Fault: QCYF: Qinghe-Chenghai-Yupaojing Fault; CSF: Chongshan Fault; LCJSZ: Lancangjiang

Suture Zone: GLGF: Gaoligong Fault.

Figure 2. (A) Simplified geological maps of the sampling areas. (B) The strata strike and dip of each sampling site

of the Oligocene Jinsichang Formation. (C) and (D), the strata strike and dip of each sampling site of the

early–middle Eocene Guolang Formation. SJ (Shibao Mountain–Jianchuan): the paleomagnetic sampling sites in

ACCEPTED MANUSCRIPT the Oligocene Jinsichang Formation. JL (Jianchuan–Laojun Mountain): the paleomagnetic sampling sites in the

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early-middle Eocene Guolang Formation.

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Figure 3. Rock magnetic results for representative samples from the Jinsichang Formation and Guolang Formation.

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(A-a) and (B-a), thermal demagnetization of IRMs that were imparted by applying a different DC field (2.4 T, 0.4

T and 0.12 T) to each of three perpendicular axes of a specimen. (A-b) and (B-b), IRM acquisition curves and DC

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field demagnetization.

Figure 4. Orthogonal projections of magnetization vector end-points for the representative specimens from the

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sampled sections. (A-a) and (B-a): the high-temperature magnetic components were isolated using the

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intersection of great circles according to the method of McFadden and McElhinny (1988). (A-b) and (B-b): the

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high-temperature magnetic components were isolated using principal component analysis (Kirschvink, 1980).

Figure 5. Equal-area projections of the site-mean directions for low-temperature magnetic components before and

after tilt correction. (A), the Oligocene Jinsichang Formation (SJ). (B), the early–middle Eocene Guolang

Formation (JL). Solid (open) symbols denote the lower (upper) hemisphere. Red stars denote the average direction

of each section with 95% confidence limit indicated by a shaded circle.

Figure 6. Equal-area projections of the site-mean directions for high-temperature magnetic components with the

95% confidence level indicated by a shaded circle before and after tilt correction. (A), the Oligocene Jinsichang

Formation (SJ). (B), the early–middle Eocene Guolang Formation (JL). In situ: the site-mean direction before tilt

correction. Tilt corrected: the site-mean direction after tilt correction. Solid (open) symbols denote the lower

ACCEPTED MANUSCRIPT (upper) hemisphere. Red stars denote the average direction of each section with the 95% confidence level indicated

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by a shaded circle.

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Figure 7. (A) The latitudinal translation with error bars versus longitudes of the localities used for paleomagnetic

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studies of the CDF. The negative (positive) value indicates southward (northward) translation. (B) The rotational

movement with error bars versus longitudes of localities used for paleomagnetic studies of the CDF. The negative

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(positive) value indicates counterclockwise (clockwise) rotation. The red lines indicate the position of left lateral

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strike-slip faults in the CDF. N-Q: middle Miocene to Pliocene; O: Oligocene; E: Eocene; P: Paleocene; U-K:

Upper Cretaceous; L-K: Lower Cretaceous. SCB: South China Block. The other abbreviations are the same as Fig.

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Figure 8. Results of E-I (elongation-inclination) correction of the Oligocene Jinsichang Formation (SJ) and the

early-middle Eocene Guolang Formation (JL). The corrected inclination for the Oligocene Jinsichang Formation is

33.9°, with an error range of 28.3－43.2°, the corrected inclination for the early-middle Eocene Guolang

Formation is 37.9°, with an error range of 31.2－44.9°. (A) Equal area projection of paleomagnetic directions; (B)

elongation direction of the curve with respect to inclination; (C) elongation/inclination as a function of f; and (D)

cumulative distribution of corrected inclination.

Figure 9. Paleomagnetic declinations obtained from the CDF, indicated by arrows, with the uncertainties shown on

both sides of the arrow. N-Q: middle Miocene to Pliocene; O: Oligocene; E: Eocene; P: Paleocene; U-K: Upper

Cretaceous; L-K: Lower Cretaceous. PDHF: Puduhe Fault; SCB: South China Block; STB: Shan Thai Block. The

other abbreviations are the same as in Fig. 1. The paleomagnetic data used in this study and in previous studies is

ACCEPTED MANUSCRIPT also listed in Table 3.

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Figure 10. (A) Structural sketch map of the southeastern edge of Tibetan Plateau. The numbers in white circles

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indicate the sequence of the initial strike-slip movement of strike-slip faults that constituted the northern-eastern

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boundary of the CDF, indicating that the XSHF-YLF constituted the northern-eastern boundary of the CDF prior to

the activity of the XJF. (B) Southward extension of the clockwise rotational movement of the CDF, and strike-slip

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movement of the boundary strike-slip faults of the CDF and Shan-Thai Block (STB) since the Oligocene. PDHF:

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Puduhe Fault; XSHF: Xianshuihe Fault; SGF: Sagaing fault. The other abbreviations are the same as in Fig. 1. Vs:

velocity of the rotational extrusion movement of the STB and the northwestern part of ICB during the period of

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32-17/12Ma; Vc1, velocity of the rotational extrusion movement of the CDF during the period of 17/12Ma-5Ma;

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Vs1, velocity of the rotational extrusion movement of the STB and the northwestern part of ICB during the period

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of 17/15Ma－5Ma. Vc1 is similar to Vs1. Vc2, velocity of the rotational extrusion movement of the CDF since the

Pliocene; Vs2, velocity of the rotational extrusion movement of the STB and the northwestern part of ICB since

the Pliocene. Vc2 is higher than the Vs2.

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Figure 1

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Figure 2

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Figure 8

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Figure 9

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Figure 10

ACCEPTED MANUSCRIPT Table 1. High temperature magnetic components of red-beds samples collected from the Oligocene Jinsichang Formation in Jianchuan area Bedding

In situ

Tilt-corrected

n/N

SJ1

26º32′/99º43′

274/18

*SJ4

26º32′/99º43′

282/8

SJ5

26º32′/99º43′

SJ7

26º32′/99º45′

SJ8

26º32′/99º45′

246/31

SJ10

26º32′/99º45′

SJ11

26º32′/99º45′

SJ13 SJ14

Average VGP

Inc.(º)

Dec.(º)

Inc.(º)

7/13

196.4

-43.1

194.0

-25.5

5/13

216.2

-37.1

214.1

-29.7

276/3

7/12

197.9

-25.4

197.6

-22.5

255/31

10/13

227.8

-55.1

203.2

-34.6

10/16

213.3

-42.6

197.8

250/39

8/14

246.7

-54.0

243/32

12/13

48.1

39.6

26º32′/99º45′

252/39

8/13

223.9

26º32′/99º45′

51/17

(º)

14.1

71.5

232.0

11.2

201.3

22.4

56.6

23.7

13.5

67.8

228.2

10.4

24.7

9.9

67.4

204.3

8.6

-22.0

53.1

6.7

67.4

228.4

5.1

207.6

-37.4

22.6

11.9

64.2

196.4

10.7

28.8

25.8

32.1

7.8

60.1

209.7

6.2

-58.4

194.4

-30.4

28.0

10.7

73.2

224.1

8.9

26.5

51.7

20.3

14.6

66.3

169.3

16.4

22.8

11.9

52.8

7.7

11.0

42.6

213.6

-46.5

8/14

Lon.( ºE)

27.2

8/11

Mean direction of Oligocene

24.7

Lat.( ºN)

9.9

8/14

200.9

-31.3

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N and n are number of samples collected and used for paleomagnetic calculation, respectively. Dec. and Inc. are declination and inclination, respectively; k is the Fisherian precision parameter for samples (Fisher 1953); α95 and A95 are the radius of cone at 95 percent confidence level about the mean direction. Average VGP is calculated by

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applying Fisher statistics on VGPs of per sampling site of the formation, Lat. and Lon. are latitude and longitude. *

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means the data was deleted from the Fisher statistics because of the huge α95

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A95

(º)

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Dec.(º)

SC

Strike/dip (º)

NU

N/E(º)

α95 k

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Locality Site

ACCEPTED MANUSCRIPT Table 2. High temperature magnetic components of red-beds samples collected from the early–middle Eocene Guolang Formation in Jianchuan area. Bedding

In situ

Tilt-corrected

n/N Strike/dip (º)

Dec.(º)

Inc.(º)

Dec.(º)

Inc.(º)

JL1

26º28′/99º49′

304/20

6/12

6.0

43.8

12.0

25.6

JL2

26º28′/99º49′

304/20

10/12

38.4

62.2

36.7

42.2

JL3 JL4

26º28′/99º50′

288/14

13/13

12.6

43.0

13.4

28.5

26º27′/99º50′

353/8

9/12

25.6

34.0

29.6

29.4

JL5

26º27′/99º51′

11/7

12/12

14.8

41.6

20.9

92.4 14.1

Average VGP

A95

(º)

Lat.( ºN)

Lon.( ºE)

(º)

7.1

72.8

236.6

5.6

56.9

185.2

12.8

13.3

51.8

5.8

73.2

229.3

4.7

19.2

12.4

60.5

205.1

10.2

40.8

81.7

5.3

70.8

194.6

5.0

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N/E(º)

α95 k

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Locality Site

26º27′/99º51′

303/11

10/13

27.0

57.5

28.3

46.5

21.8

11.3

64.8

180.3

11.6

26º27′/99º51′

66/8

10/13

18.9

45.1

14.2

39.0

9.1

18.5

76.3

205.6

17.0

JL8

26º41′/99º55′

351/12

11/13

37.3

46.4

44.3

37.2

21.1

10.2

49.2

188.5

9.2

SC

JL6 *JL7

26º41′/99º54′

268/5

10/12

215.0

-24.8

213.8

-20.8

22.2

10.6

54.4

210.0

8.1

26º41′/99º54′

135/8

10/12

24.1

9.3

23.4

16.8

41.7

7.6

61.4

224.8

5.6

JL14

26º41′/99º53′

126/8

6/10

215.8

-19.0

215.8

-27.0

98.1

6.8

54.4

203.0

5.5

NU

JL10 JL12

26º40′/99º52′

134/4

9/11

226.8

-27.8

227.0

-31.8

19.4

12.1

45.6

192.1

10.2

26º40′/99º52′

116/2

9/12

206.0

-33.7

205.9

-35.7

40.6

8.2

65.3

200.6

7.2

JL18

26º40′/99º51′

179/4

14/14

212.9

-34.9

210.5

-37.1

86.7

4.3

61.5

194.8

3.9

JL19

26º40′/99º51′

194/4

11/11

218.2

-37.4

215.3

-39.0

53.2

6.3

57.6

189.8

5.8

JL20

26º39′/99º52′

74/8

7/12

216.8

-17.4

219.1

-22.1

29.6

11.3

50.3

204.7

8.7

JL21

26º38′/99º51′

71/6

5/10

199.7

-20.4

201.3

-25.0

27.1

15.0

65.9

219.8

11.8

22.9

7.9

29.7

32.0

44.9

5.6

D

TE 16/21

Mean direction of Oligocene

MA

JL16 JL17

16/21

28.8

35.0

AC CE P

N and n are number of samples collected and used for paleomagnetic calculation, respectively. Dec. and Inc. are declination and inclination, respectively; k is the Fisherian precision parameter for samples (Fisher, 1953); α95 and A95 are the radius of cone at 95 percent confidence level about the mean direction. Average VGP is calculated by applying Fisher statistics on VGPs of per sampling site of the formation, Lat. and Lon. are latitude and longitude. * means the data was deleted from the Fisher statistics because of the huge α95

ACCEPTED MANUSCRIPT

Table 3. The Cretaceous and Paleogene reference paleopoles of the East Asia from the Apparent Polar Wander Path of East Asia (Cogné et al., 2013). Paleopole

Age

Average Paleopole

N Lon.( ºE)

k

A95 (º)

89.2

257.8

-

7.6

106.7

2.8

249.6

-

6.9

247.5

57.4

4.1

89.0

276.6

200.7

5.4

12.4

21

87.5

257.3

154.8

2.6

23.7

25

83.9

259.6

106.7

2.8

83.9

41.7

14

81.9

260.8

94.8

4.2

55.0

13

81.6

238.8

51.6

5.9

65.2

22

81.9

247.5

57.4

4.1

81.9

77.3

45

79.7

219.5

42.6

3.3

79.7

44

79.5

216.9

42.2

3.4

87.8

53

77.9

212.8

46.2

2.9

105.1

16

82.2

205.4

118.1

3.5

109.8

22

80.8

199.5

78.9

3.5

121.6

41

80.6

126.2

44

79.9

L-K

MA

NU

81.9

D

U-K

A95 (º)

5

E

P

k

192.9

60.4

2.9

193.5

70.0

2.6

RI

O

Lon.( ºE)

1.0 N-Q

Reference

Lat.( ºN)

SC

Lat.( ºN)

TE

(Ma)

PT

Time

259.6

Cogné et al., 2013

79.0

216.2

-

1.8

80.9

197.4

-

1.5

AC CE P

N-Q: middle Miocene to Pliocene; O:Oligocene; E: Eocene; P: Paleocene; U-K: Upper Cretaceous; L-K: Lower Cretaceous; N: Number of data in the statistics; Lat.: Latitude of paleopole; Lon.: Longitude of paleopole; k: the Fisherian precision parameter for samples (Fisher, 1953); A95 is the radius of cone at 95 percent confidence level about the average paleopole.

ACCEPTED MANUSCRIPT

Table 4. Cretaceous and Cenozoic paleomagnetic data yield from the CDF. Time

N

Dec. (º)

Expected

Inc. (º)

α95 (º)

Dec. (º)

Inc. (º)

Average VGP Lat ( ºN)

PT

Location (ºN/ºE)

Lon ( ºE)

Relative to East Asia

A95 (º)

K

-

RI

Observe Name

2.8

76.3

259.0

1.3

68.5

210.5

6.2

Rotation (º)

Translation (º)

Reference

Data yield from the west side of the YLF N-Q

17

1.4

27.8

1.1

0.4

43.0

26.3/100.0

N-Q

-

5.0

25.5

1.7

0.3

43.7

Jianchuan(SJ)

26.55/99.30

O

8

200.9

– 31.3

7.7

2.2

37.2

200.9

– 33.9 (–43.2 ~ –28.3)

26.53/99.75

E

16

29.7

32.0

29.7

37.9 (31.2~44.9)

5.6 5.6

4.3

35.3

MA

Jianchuan(JL)

79.1

266.7

SC

25.7/101.9

Dali

NU

Yuanmou

61.1

201.6

5.1

81.4

53.6

2.6±6.5

9.8±5.9

Zhu et al., 2008

4.7±6.3

12.1±5.7

Li et al., 2013

18.7±7.1

3.9±5.4

This study

– 4.4 ~2.2 ~5.7

This study (inclination shallowing corrected)

25.4±9.1

-

1.9±6.9

This study

–7.0~ –1.8 ~2.6

This study (inclination shallowing corrected)

25.8/101.5

P

9

25.8

28.6

5.5

4.8

34.6

63.7

210.1

4.5

-

21.0±4.7

3.8±4.5

Yang et al., 2001

25.7/101.3

P

10

16.6

31.1

4.8

4.8

34.4

72.2

218.2

4.0

-

11.8±4.4

2.1±4.2

Yoshioka et al., 2003

Dayao(modified)

25.7/101.3

p

7

21.1

31.4

5.3

4.8

34.4

68.5

211.1

4.4

-

16.4±4.6

1.9±4.4

Yoshioka et al., 2003

26.1/101.7

P

16

17.2

26.6

26.1/101.7

P

12

22.6

26.6

Zhupeng

25.9/101.8

P

15

25.4

34.3

Chuxiong

25.0/101.5

L-K

21

44.6

41.3

27.9/102.3

L-K

13

2.8

Xichang

27.9/102.3

U-K

20

4.2

Huili

26.8/102.5

L-K

7

22.1

Huidong

26.5/102.4

U-K

18

8.1

Huidong

26.4/102.3

P

7

178.7

Bailu

25.7/102.1

P

6

30.7

4.8

35.0

69.9

225.2

4.6

-

12.4±4.7

5.3±4.5

Yoshioka et al, 2003

4.8

35.0

65.5

217.0

4.6

-

17.9±4.7

5.4±4.5

Yoshioka et al., 2003

3.4

4.8

34.8

65.5

203.4

2.9

-

20.6±3.9

0.3±3.7

Otofuji et al. 1998

10.7

9.9

41.3

49.5

183.6

10.2

-

34.7±8.3

0.0±7.6

Funahara et al. 1992

1.5±4.0

Tamai et al., 2004

Data yield from the east side of the YLF

4.7

10.9

40.4

83.7

244.2

4.4

-

－6.7±3.8

0.1±3.5

Tamai et al.,2004

37.1

3.8

10.1

43.9

68.9

204.5

3.4

-

12.0±2.9

4.9±2.7

Huang and Opdyke, 1992

38.8

6.6

10.8

38.5

81.3

222.6

6.1

-

－2.7±5.0

– 0.2±4.7

Huang and Opdyke, 1992

43.3

5.3

10.2

45.2

86.3

238.5

5.2

-

－7.3±4.4

40.2

AC

Xichang

5.8

5.8

CE

*Yongren Yongren(modified)

PT ED

Dayao *Dayao

– 13.7

12.1

4.9

35.6

70.5

285.6

8.8

-

－6.0±7.2

12.7±7.1

Huang and Opdyke, 1992

38.9

10.6

4.9

34.5

61.7

193.1

9.7

-

25.9±8.3

– 3.0±7.7

Otofuji et al. 1998

Rotation: the negative value means counterclockwise rotation, the positive value means clockwise rotation. Translation: the negative value means southward translation, the positive value means northward translation. Lat. and Lon. are latitude and longitude; Age: N-Q, middle Miocene to Pliocene; O, Oligocene; E, Eocene; P, Paleocene; L-K, Lower Cretaceous; U-K, Upper Cretaceous; N is the number of sampling sites used for paleomagnetic calculation. Dec. and Inc. are declination and inclination, respectively; α95 and A95 is the radius of cone at 95 percent confidence level about the mean direction; K is the Fisherian precision parameter (Fisher, 1953); Average VGP is calculated by applying Fisher statistics on VGPs of per sampling site of the formation.* means the problematic paleomagnetic data.

ACCEPTED MANUSCRIPT Highlights Paleogene paleomagnetic data was yield from the Chuan Dian Fragment (CDF).

2.

The Western and middle part of CDF experienced integral clockwise rotation.

3.

The clockwise rotational movement of CDF gradually spread eastward.

4.

Evolution of strike-slip faults were controlled by rotational movement of CDF.

AC CE P

TE

D

MA

NU

SC

RI

PT

1.