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RESEARCH Slip Rate and Recurrence Intervals of The RESEARCH Slip rate and recurrence intervals of the east Lenglongling fault constrained by morphotectonics: Tectonic implications for the northeastern Tibetan Plateau Wenliang Jiang1, 2,*, Zhujun Han2, Peng Guo2, Jingfa Zhang1, Qisong Jiao1, Shuai Kang1, and Yunfeng Tian1 1KEY LABORATORY OF CRUSTAL DYNAMICS, INSTITUTE OF CRUSTAL DYNAMICS, CHINA EARTHQUAKE ADMINISTRATION (CEA), BEIJING 100085, CHINA 2INSTITUTE OF GEOLOGY, CHINA EARTHQUAKE ADMINISTRATION (CEA), BEIJING 100029, CHINA ABSTRACT The Lenglongling fault located in the northeast margin of the Tibetan Plateau plays an important role in accommodating the tectonic defor- mation of the Tibetan Plateau relative to the Gobi–Ala Shan platform to the north and the North China craton to the east. However, little is known about the fault due to a lack of previous research. In this study we use terrestrial light detection and ranging (LiDAR) data combined with high-resolution remote sensing images to survey offset landforms in the east part of the Lenglongling fault. Microtopographic analysis of well-preserved offset terraces, gullies, ridges, and pluvial fans in the highland environment allows evaluation of single-event slip and multievent cumulative slip. Our study provides an important assessment of the horizontal offset associated with the latest earthquake and four paleoearthquakes that were identified from a series of offset bedrock terraces by constructing a morphotectonic evolution model. Terrestrial LiDAR data indicate that the east Lenglongling fault follows a characteristic slip model. The single-event slip of this section is ~9.4 m; 7–8 paleoearthquakes are thought to have occurred during the Holocene, and a left-lateral strike-slip rate of 6.6 ± 0.3 mm/yr is estimated. Combining the slip rate and the single-event slip distribution, we determine a mean recurrence interval of 1430 ± 140 yr for past earth- quakes along the east Lenglongling fault. This result is similar to that of the adjacent Gulang fault, but differs slightly from those of other adjacent faults, which may mean that the Lenglongling and Gulang faults compose an integral fault zone. The large number of millennial recurrent active faults in this region heightens the risk of future seismic activity in the northeast Tibetan Plateau. LITHOSPHERE; v. 9; no. 3; p. 417–430 | Published online 14 February 2017 doi:10.1130/L597.1 INTRODUCTION section of the Qilian-Haiyuan fault zone (Gaudemer et al., 1995). Only two earthquakes have been recorded here, both M 6.4, in 1984 and 2016. The Lenglongling fault (LLLF) is located in the northeastern margin However, a series of offset landforms has been identified from high- of the immense arcuate tectonic zone of the Tibetan Plateau (Fig. 1B). resolution remote sensing (HRRS) images, as well as in the field (He et Together with the Tuolaishan, Jinqianghe, Maomaoshan, Laohushan, and al., 2000; Lasserre et al., 2002), that imply that several strong earthquakes Haiyuan faults, the LLLF is part of the Qilian-Haiyuan fault zone (Zheng struck the LLLF during the Holocene. Single-event slip, mean slip rate, et al., 2013) (Fig. 1A), an important left-lateral strike-slip fault system and recurrence intervals of the LLLF are all important parameters for in the northeastern Tibetan Plateau. This active tectonic zone accommo- evaluating the future seismic hazard of this region, for understanding the dates eastward movement of Tibet relative to the Gobi–Ala Shan platform regulatory mechanism of the LLLF in terms of the tectonic deformation (GASP) to the north (Tapponnier and Molnar, 1977; Zhang et al., 1988a, of the northeastern Tibetan Plateau, and for constraining the dynamics 1988b). Many strong earthquakes have previously occurred in this region, of the Tibetan Plateau (Molnar and Tapponnier, 1975; Avouac and Tap- including the 1920 Haiyuan (M 8.5) and the 1927 Gulang (M 8–8.3) ponnier, 1993; England and Molnar, 1997). earthquakes. Nevertheless, we know very little about the LLLF compared In order to more accurately estimate single-event slip and recurrence with the surrounding active faults due to lack of observations. Our current intervals, we carried out field work in the eastern part of the LLLF. Ter- knowledge of the slip rate is controversial, as it spans a large range from restrial light detection and ranging (LiDAR) is used to measure the detailed 4 to 19 mm/yr (Gaudemer et al., 1995; He et al., 2000; Lasserre et al., offset landforms along with the analysis of HRRS images. The LLLF is 2002; He et al., 2010; Zheng et al., 2013). A 220-km-long seismic gap located in high-altitude regions, where primary geologic landforms are with significant potential hazard has been identified along the western preserved without damage from human activity. Markers of pre-earthquake morphology that are linked across the fault, such as terrace risers and gul- Wenliang Jiang http://orcid.org /0000 -0002 -2006 -4605 lies, are identified and analyzed in order to constrain the surface rupture *[email protected] history. Single-event slip and multievent cumulative slip are estimated to LITHOSPHERE© 2017 Geological | Volume Society 9 of| AmericaNumber 3| |For www.gsapubs.org permission to copy, contact [email protected] 417 Downloaded from http://pubs.geoscienceworld.org/gsa/lithosphere/article-pdf/9/3/417/999110/417.pdf by guest on 27 September 2021 WENLIANG JIANG ET AL. 80°0'0"E 100°0'0"E 120°0'0"E B Gobi-Ala Shan "N A '0 LSSF Wulumuqi Platform Gobi-Ala Shan Platform °0 Fig.1A S Beijing 40 Minle AEJF SG North China DK Yo ngchang LF Xining Craton TL ML-YCF XS "N SFXi'an SF Tibetan Plateau HF '0 Qilian SN ML LM -Q -D °0 LF MY Chengdu 30 N Lhasa F 0" 0' HH 06300k00 m F "N 38° '0 HC-STF °0 20 NE Fig. Ti 2 RY be LL Gulang LF F SF ta GL n Pl Menyuan at Gangca ea J QHF u MMS Jingtai Historical F Earthquake (Ms) Tianzhu "N HY '0 F 5.0-6.0 Datong °0 Haiyan Huzhu 37 6.1-7.0 Yo ngdeng 0315 0 km 7.1-8.5 100°0'0"E 102°0'0"E 104°0'0"E Figure 1. Geological setting of the Lenglongling fault. (A) Focal mechanism of an earthquake with M 6.4 showing reverse-type kinematics is shown. Red line denotes the Lenglongling fault (LLLF). Black lines show the distribution of the surrounding major faults: GLF—Gulang fault; JQHF—Jinqianghe fault; MMSF—Maomaoshan fault; HYF—Haiyuan fault; SN-QLF—Sunan-Qilian fault; TLSF—Tuolaishan fault; RYSF—Riyueshan fault; ML-YCF—Minle- Yongchang fault; ML-DMYF—Minle-Daminying fault; HC-STF—Huangcheng-Shuangta fault; LLSF—Longshoushan fault (faults are modified from Deng et al., 2003). (B) Inset showing the location of A in the northeastern Tibetan Plateau. White rectangle shows the location of Figure 2 along the Lenglongling fault. Fault abbreviations: LMSF—Longmenshan fault; AEJF—Altun Tagh fault; DKLF—Dongkunlun fault; XSHF—Xianshui River fault; SGS—Shanxi graben system; HHF—Honghe fault. quantitatively determine the slip distribution model and the occurrence from the major branch, according to its epicenter depth and the geological of paleoearthquakes. By combining this information with previous dat- map. The 1927 earthquake (M 8.0) of Gulang occurred to the east of the ing results, we derive the slip rate and recurrence interval of the LLLF. LLLF (Gaudemer et al., 1995). According to historical evidence, a strong earthquake that hit the middle of the Gansu area is thought to be related GEOLOGICAL SETTINGS to the LLLF (Liu et al., 1998). Quaternary glacial and periglacial processes have strongly contributed The northeastern Tibetan Plateau has undergone strong tectonic deforma- to shaping the landforms of northeastern Tibet (Derbyshire et al., 1991; tion since the Cenozoic Era (Yin et al., 2008). Widespread folding, thrusting, Lehmkuhl et al., 1998; Van Der Woerd et al., 2000, 2002), including the and strike-slip faulting in the Paleogene, Neogene, and Quaternary Periods Lenglongling Mountains. Glacial cirques, some still occupied by glaciers, indicate that this region has been undergoing crustal shortening and shear glacial valleys, glaciofluvial tills, and moraines, can be identified along slip, as well as vertical uplift, which has resulted in typical basin-range the entire LLLF. Glaciation in the Lenglongling area is divided into two structures (Molnar and Tapponnier, 1975; Meyer et al., 1998; Tapponnier stages: the new ice age and the last glaciation (prior to 11 ka) (Wu, 1984). et al., 1990, 2001; Yuan et al., 2004). Two groups of structures trending The last glaciation is divided into three stages (Kang et al., 1992), two west-northwest and north-northwest make up the tectonic framework of of which are large-scale glacial advances that occurred before 38,000 yr the northeastern Tibetan Plateau. The Qilian-Haiyuan fault zone, one of ago, and between 38000 and 18,000 yr ago, respectively. Between 14,000 the most important of the NWW-trending structures, consists of a series of and 12,665 yr ago there was a short-term pause in glaciation, which left-lateral en echelon active faults with slight thrust movement from south represents the third stage; the new ice age occurred in China ca. 3110 yr to north. The LLLF is located in the middle segment of the Qilian-Haiyuan ago (Kang et al., 1992). fault zone and is predominantly a left-lateral strike-slip fault that had oblique slip in the west during the Quaternary (Gaudemer et al., 1995). Although the METHODOLOGY AND DATA LLLF is less studied, it has undergone strong seismic activity in the Holo- cene, evidenced by a series of offset landforms including streams, terraces, Trench excavation is the most common method for estimating the behav- moraines, and ridges (He et al., 2000; Lasserre et al., 2002; He et al., 2010).
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