at SciVerse ScienceDirect

Marine and Petroleum Geology 39 (2013) 48e58

Contents lists available

Marine and Petroleum Geology

journal homepage: www.elsevier .com/locate/marpetgeo

Paleozoic fault systems of the Tazhong Uplift, Tarim Basin, China

Chuanxin Li a,b,*, Xiaofeng Wang c, Benliang Li d, Dengfa He a

a School of Energy Resources, China University of Geosciences, Beijing 100083, ChinabResearch Institute of Petroleum Exploration and Development e Langfang, CNPC, Guangyang Street, Langfang 065007, Hebei Province, Chinac Tarim Oil Company, CNPC, Korla 841000, ChinadResearch Institute of Petroleum Exploration, CNPC, Beijing 100083, China

a r t i c l e i n f o

Article history:Received 14 December 2011Received in revised form20 September 2012Accepted 29 September 2012Available online 30 October 2012

Keywords:Fault systemsStrike-slip faultMagmatic plugsTazhong UpliftTarim Basin

* Corresponding author. Research Institute of Petropment e Langfang, CNPC, Guangyang Street, LangfChina. Tel.: þ86 10 69213094; fax: þ86 10 69213417.

E-mail address: chuanxin_li@163.com (C. Li).

0264-8172/$ e see front matter � 2012 Elsevier Ltd.http://dx.doi.org/10.1016/j.marpetgeo.2012.09.010

a b s t r a c t

This report presents interpretations developed from a detailed study of new three-dimensional (3-D)high-resolution reflection seismic data in a portion of Tarim Basin. The tectonic history began withoceanic spreading during the CambrianeEarly Ordovician and continues beyond the SilurianeDevoniantime of oceanic closure. Paleozoic faults of the Tazhong Uplift in the hinterland of Tarim Basin are cappedby thick and undisturbed Meso-Cenozoic sedimentary sequences. Four Paleozoic fault systems have beenrecognized: (1) the CambrianeEarly Ordovician extensional faulting, (2) the Late Ordovician NWWtrending thrust faulting, (3) the SilurianeDevonian NNE strike-slip faulting and (4) the Permian plu-tonism influenced by pre-existing fault planes. Zones of weakness created during CambrianeEarlyOrdovician extensional faulting influenced subsequent tectonic movements. The Late Ordovician faultsystem divides the Tazhong Uplift into several deformation zones. Their mechanical characteristics varyacross the study area, with stronger thrusting in the east. The SilurianeDevonian strike-slip fault systemconsists of three components: main faults, subordinate en echelon faults, and fault troughs. The mainfaults appear as steeply dipping, almost vertical, offsets on seismic map view, with associated flowerstructures on seismic profiles, together with other levels of faults. The Permian magmatic plugs havea spotty or bandy distribution, and are interpreted to have utilized former faults.

� 2012 Elsevier Ltd. All rights reserved.

1. Introduction

Fault systems and their distribution play important roles inbasin architecture, geomorphology and geography. At the sametime, they often have a key influence on hydrocarbon migrationand accumulation in a petroliferous basin. The Tazhong Uplift islocated in the central Tarim Basin (Jia et al., 1995; Jia, 1997), and isone of the most important exploration areas. Few researchersfocused on Paleozoic fault systems of the Tarim because they arecovered by several kilometers of undisturbed Meso-Cenozoicsedimentary sequences that underlie the Taklimakan Desert (Luand Hu, 1997; Zhang and Jia, 1997).

With the development of deep hydrocarbon exploration, themarine Ordovician carbonate reservoirs in Tazhong Uplift havebeen recognized as the prime exploration target in the area.Petroleum geologists have paid more attention to Paleozoic

oleum Exploration & Devel-ang 065007, Hebei Province,

All rights reserved.

structure and begun to realize the complexity of Paleozoic faultsystems (Zhang et al., 2002; Li et al., 2004, 2006; Wu et al., 2005,2010a, 2010b, 2012; Zhao et al., 2006; Sun et al., 2007; Li et al.,2008; Zhou et al., 2011; Lin et al., 2012). They provide importantoil and gas migration channels, but also have a major influence onreservoir development, particularly on karst reservoirs in theYingshan Formation, early Ordovician and the reef-shoal reservoirsof the Lianglitage Formation, late Ordovician. However, due to thelimitations of early low-resolution seismic data, few integratedstudies focused on the fault distributions, structural styles, tectonicstages and dynamic mechanisms in the central Tarim Basin.

New borehole, log and seismic data have been obtained duringrecent exploration and development of Tazhong Uplift. Of greatimportance is the acquisition and processing of continuous high-resolution 3-D seismic coverage data, collected by the Tarim OilCompany, CNPC. These seismic data covering an area of 4500 km2

provide detailed subsurface information and make it feasible tocarry out a regional structural analysis (Li et al., 2009, 2010).

In this paper, characteristics, distribution and dynamic mecha-nisms of Paleozoic faulting are discussed on the basis of compre-hensive interpretations of the new 3-D data. This study used anintegrated database that included eight 2D seismic profiles across

C. Li et al. / Marine and Petroleum Geology 39 (2013) 48e58 49

the Tazhong uplift and more than 100 well logs, which providea firm basis for the recognition and mapping of the major faultsystem that can be recognized on seismic profiles.

2. Geological setting and stratigraphy

The Tarim Basin, with an area of about 560,000 km2, is thelargest petroliferous basin of China. It is surrounded by the Tian-shan Mountains to the north, the western Kunlun Mountains to thesouth, and the Altyn Mountains to the southeast (Fig. 1). Based onthe interpretation of a grid of two-dimensional (2D) seismic data,Tarim basin is divided into seven major structural units includingthree uplifts and four depressions (Jia, 1997), that is the Kuqadepression, the Tabei uplift belt, the North depression belt (theManjiaer and the Awati depressions), the Central uplift belt, theSouthwestern depression belt, the Tadong uplift belt and theSoutheast depression (Fig. 1). The Tazhong uplift, trending NWeSE,is located at the Center uplift belt with an east-west length of 250e300 km and a south-north length of about 50 km.

The geodynamic setting of the Tarim block has significantimpact on the Paleozoic fault systems in the Tazhong uplift (Fig. 2).The Tarim basin may have experienced intensemulti-stage tectonicactivities in Paleozoic period (Nakajima et al., 1990; Allen et al.,1992; Jia, 1997). The evolutional process can be divided into thefollowing four main phases. (1) From Precambrian to the EarlyOrdovician, the Tarim block broke away from Rodinia superconti-nent and the Kudi and South Oceans were formed (Fig. 2a). Duringthe late Proterozoic to the Early Paleozoic, the Kudi Ocean devel-oped between the Kunlun block and the Tarim block (Luo et al.,2005; Mattern and Schneider, 2000; Wang, 2004). The suturezone of the ocean was found in the Kudi Area along the westernKunlun Mountains (Wang, 2004; Zhang et al., 2007; Xiao et al.,2005). In the early Paleozoic period, the Tarim block broke awayfrom the Rodinia supercontinent, the north Tarim block stretchedand formed the South Tianshan Ocean gradually, and the southTarim block developed Paleo-Tethys trench-arc-basin system (Xuet al., 2005, 2009; Zhang et al., 2009, 2010; Wang et al., 2010). In

Figure 1. Tectonic outline of Tarim Basin and digital elevation map of S

this extensional setting, some half-grabens or grabens developed inthe south-central Tarim Block. The Manjiaer depression (Fig. 2a riftor an aulacogen) developed in this period (Jia, 1997; Gao et al.,2009; Wu et al., 2010b). The deep trough was controlled by theextensional faults and filled with several thousand meters of thickmarine deposits in the Early Paleozoic. (2) From the Middle Ordo-vician to the Late Ordovician, the Tarim basin evolved from passivecontinental margin and intra-cratonic depression to a peripheralforeland or retroarc foreland environment (Fig. 2b), with thesubduction of the Paleo-Tethys Ocean (Kudi Ocean) from the southto north (Zhang et al., 2002; Li et al., 2009). The timing of thecompressive deformation and uplift in the south central basin wascoeval with the closure of the Kudi Ocean (Li et al., 1996; Wei et al.,2002; Lin et al., 2008, 2009). The forming of the Tazhong upliftresulted from compression of the Tarim block, a result of thesubduction of Kudi Ocean on the west side of Tarim block in theMiddle Ordovician (Zhang et al., 2002; Li et al., 2009). The Tazhonguplift is formed at this time (Li et al., 1996; Wang, 2004; Wei et al.,2002; Lin et al., 2008, 2009) and lies in the frontal zone of thetectonic compression in this period. The uplift in the Late Ordovi-cian has caused the widely distributed high-angle unconformity atthe southwestern to southeastern basin margins. (3) From Silurianto Devonican period, the persistent compression exited betweenthe Tarim Block and the Kunlun Block, and regional unconformityand faults formed (Fig. 2c). The south Tairim basin in this period isregarded as a foreland basin with the huge thickness marine flyschdeposition in the foredeep of the West Kunlun Area. The intensethrusting in late Devonian was one of the most important tectonicmovements in the Tarim basin evolutional history. At the end of theDevonian, the thrusting from the south Tarim passed through theSouthwest depression and transferred to the Tazhong uplift Area,and the continuous compressive stress resulted in NNE strike-slipfaults (Wu et al., 2009, 2012). As a result, the Devonian, Silurian,and even Ordovician strata were eroded and formed the mostimportant unconformity in the study area (Lin et al., 2008, 2009).(4) The tectonic activities in Carboniferous have characteristics ofintegral uplifting, and its intensity was much weaker than Late

outheast Asia with the studying area in the center of Tarim Basin.

Figure 2. Schematic map showing the tectonic setting of the Tarim Basin (modified from Lin et al., 2012). TB: Tarim Block; KB: Kunlun Block; YB: Yili Block; KO: Kudi Ocean (Paleo-Tethys Ocean); TO: Neo-Tethys Ocean; SO: South Tianshan Ocean; NO: North Tianshan Ocean; KDS: Kudi suture; TZU: Tazhong Uplift; MJED: Manjiaer depression (northdepression).

C. Li et al. / Marine and Petroleum Geology 39 (2013) 48e5850

Ordovician or the SilurianeDevonian period. So the Carboniferousstrata (Tg3) are widely distributed across the study area. Its thick-ness is uniform, with a slightly thickening trend from northwest tosoutheast, indicating a period of tectonic quiescence. The Permianmagmatic activities were related to the evolution of Paleo-TethysOcean (Chen et al., 1997, 2006; Yang et al., 2005). Permian volcanicrocks are encountered in most wells of the Tazhong uplift witha thicknesses ranging from tens of meters to over one hundredmeters. Upper part of these rocks is generally tuff, and lower part isbasalt. Faulting during this time is considered to be associated withmagmatic intrusion and ceases with their termination.

The Tazhong uplift Area is underlain by rocks of the PaleozoicErathem that generally comprises the Cambrian System to thePermian System (Jia, 1997) (Fig. 3). The Lower Cambrian Seriesconsists of a succession of gray to dark gray limestone and dolomitewith intercalated black or purple shale. The Middle to UpperCambrian contains thick gypsum and salt layers and thick-beddeddolomites, which are characteristic of an evaporative carbonateplatform environment. The Ordovician carbonate system ispredominantly composed of thick limestones and dolomites of anopen platform with reef and shoal deposits. There is an unconfor-mity between the Middle and the Upper Ordovician, which devel-oped mainly in the central uplift belt, where the Lower OrdovicianYingshan formation is overlain by the Upper Ordovician Lianglitageformations. There is a widespread angular unconformity betweenthe Silurian and the Ordovician systems. The Silurian System ischiefly composed of sandstone and mudstone of tidal-flat faciesthat decreases in thickness from west to east, having the charac-teristics of downlap and top truncation in seismic profiles. TheDevonian System is absent in most of Tazhong uplift Area, whichcharacterized by thick-bedded red sandstone. The CarboniferousSystem shows overlap eastwards on seismic profiles. It is largelycomposed of sandstone and mudstone with intercalated limestoneand bioclastic limestone. The Permian System consists of gray orbrown sandstone and mudstone with intercalated volcanics.

3. Stages of fault deformation

There have been many methods to estimate the forming time offault based on seismic profiles, such as the age anlaysis of theunconformities, syntectonic strata and fault-stratum contact rela-tion. However, it is usually difficult to use only these data toquantitatively evaluate the forming time of the fault. Four stages offaulting have been interpreted using the new 3-D seismic data

across Tazhong Uplift. The stages are: extensional faulting in theCambrianeEarly Ordovician; thrust faulting in the Late Ordovician;northeastward strike-slip faulting in the SilurianeDevonian; andfaulting associated with the Permian magmatic plugs (Fig. 4).

3.1. Unconformities

Fault deformation and the development of unconformitysurfaces are interrelated products of the same tectonic adjust-ments. This is interpreted to be the case within the study area.Consequently, a study of the unconformity surfaces has led tobetter understand the stages of tectonism (Fig. 5).

Tarim Basin experienced a long period of tectonic evolutionduring which several significant unconformity surfaces developed(He et al., 2005; Lin et al., 2012) and Lin et al. (2012) described threewidespread angular unconformities. The first developed during themiddle of the Ordovician, the second during the late Ordovician,and the third during the early Devonian to Carboniferous. In thestudy area, four unconformities from the Cambrian to theCarboniferous have been identified on the seismic sections (Fig. 5):(1) the Cambrian/Precambrian unconformity (Fig. 3, Tg7), on whichthe overlying Cambrian has continuous events in seismic reflec-tions; (2) the Upper Ordovician/Lower Ordovician unconformity(Fig. 3, Tg52), which separates the overlying Upper Ordovicianwithits continuous seismic reflections, from the underlying erodedLower Ordovician whose internal seismic signature is one ofrandom wave groups with weak amplitudes; (3) the Silurian/Ordovician unconformity (Fig. 3, Tg5), one of the most significantunconformities in Tarim Basin, formed during the Late Ordovicianperiod, the Silurian or even the Carboniferous is in direct contactwith the underlying Upper Ordovician; and (4) the Carboniferous/Silurian unconformity (Fig. 3, Tg3), another significant unconfor-mity in whole Tarim Basin, during whose formation the Devonianand the Upper Silurian, even the entire Silurianwere removed frommost of Tazhong uplift Area so that the Carboniferous with strongamplitudes and continuous events in seismic reflections liesdirectly on Ordovician strata.

3.2. Syntectonic strata

Syntectonic strata record dynamic processes of tectonic defor-mation. In recent years, theories and techniques of refined structuralgeometric analysis have developed rapidly, as has the quantitativeanalysis of fault-related folds (Suppe, 1983; Shaw et al., 2005).

Figure 3. Comprehensive stratigraphic column of the Tazhong Uplift (derived from Tarim Oil Company, CNPC).

C. Li et al. / Marine and Petroleum Geology 39 (2013) 48e58 51

Strata, interpreted here as syntectonic strata, are clearly evidenton seismic sections along the Tazhong Uplift (Fig. 5). Tazhong No. 1Fault propagatesupwards fromthebasement, forminga fault-relatedfold in the CambrianeOrdovician strata and syntectonic strata of theUpper Ordovician Sangtamu Formation (Tg51 toTg5) and one part ofthe Silurian. Seismic data shows the syntectonic strata to be thinneron thehangingwall thanon the footwall, anda characteristic growthtriangleboundedbyanactiveandan inactive axis.As theTazhongNo.1 Fault propogated upwards the axes converged, and narrowed thegrowth triangle located between them.

Growth strata are identified as the Sangtamu Formation of theUpper Ordovician (Tg5 to Tg52) and the overlying Silurian strata(Fig. 5, Tg5 to Tg3). From this, the times of the correspondingfaulting are constrained to the Late Ordovician and the SilurianeDevonian age.

3.3. Fault-stratum contact relation

A common method of determining the timing of deformation isto consider a fault’s relationship with neighboring stratigraphy. Afault is younger than the strata it offsets and older than thatterminates it. Therefore, the time of a fault’s most recent, or last,

movement is determined by indentifying the youngest offset strataand the oldest terminating it (Figs. 6e10). The SW to NE trendingstrike-slip faults are seen to offset seismic reflecting layer Tg5, thebase of Silurian strata, and terminate at Tg3, the base of theCarboniferous, so are interpreted to have last moved during theSilurianeDevonian. The intrusion timing of magmas has beendetermined as Permian in the same way.

4. Structural characteristics and distribution of the Paleozoicfaulting

As stated above, the faulting systems in Tazhong uplift Area havebeen interpreted as four stages. Faults developed at different stagesare apt to develop where earlier faults have created zones ofweakness. In these instances, older faults can be superposed ordeformed by younger ones. Many of the faults in the study area areinterpreted to be examples of such multiple stages development.

4.1. Extensional faulting in the CambrianeEarly Ordovician

Extensional faults of CambrianeEarly Ordovician have beeninterpreted on 3-D seismic profiles (Figs. 6e9, shown in green). It is

Figure 4. a. Map showing the distribution of Paleozoic faults of Tazhong Uplift (the faults are projected to the Tg6). b. The coherent image of the top of the Cambrian (Tg6) on theTazhong well group 45. Faults are in their color definitions: CambrianeEarly Ordovician in green, Late Ordovician in red, SilurianeDevonian in purple and the faults associated withPermian magmatic plugs in cyan. (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.)

Figure 5. Seismic profile across the Tazhong Uplift showing the unconformities and growth strata. Dash lines indicate unconformities; the tops in the profiles are calibrated by thewell log data and the representative strata of the seismic sequences can be seen from Figure 3. Tg: Top of the Permian System; Tg3: Top of the Devonian System; Tg5: Top of the lateOrdovican Sangtamu Formation; Tg51: Top of the late Ordovican Lianglitage Formation; Tg52: Top of the early Ordovican Yingshan Formation; Tg6: Top of the Cambrian System;Tg61: Top of the Middle Cambrian Awatage Formation.

C. Li et al. / Marine and Petroleum Geology 39 (2013) 48e5852

Figure 6. Seismic profile across the western Tazhong Uplift showing fault and stratigraphy interpretations. See Figure 4: AeA0 for location. Dash lines indicate unconformities;Faults are in their color definitions: CambrianeEarly Ordovician in green, Late Ordovician in red, SilurianeDevonian in purple and the faults associated with Permian magmaticplugs in cyan. The tops in the profiles are calibrated by the well log data and the representative strata of the seismic sequences can be seen from Figure 3. Tg: Top of the PermianSystem; Tg3: Top of the Devonian System; Tg5: Top of the late Ordovican Sangtamu Formation; Tg51: Top of the late Ordovican Lianglitage Formation; Tg52: Top of the earlyOrdovican Yingshan Formation; Tg6: Top of the Cambrian System; Tg61: Top of the Middle Cambrian Awatage Formation. (For interpretation of the references to colour in this figurelegend, the reader is referred to the web version of this article.)

C. Li et al. / Marine and Petroleum Geology 39 (2013) 48e58 53

formed along the border between the Tazhong uplift and theManjiaer depression. The extensional faults resulted in sedimen-tary thickening of the platform-margin and the formation of Taz-hong No. 1 fault belt. Under the influence of late tectonicmovement, the extensional faulting can be reformed and compli-cated. Seen from the profile DeD0 in the eastern potion of Tazhonguplift Area (Figs. 4 and 9); the thickness of CambrianeEarly Ordo-vician is about 3600 m (from bottom of Cambrian to the Top of theearly Ordovician Yingshan Formation) in slope-shelf zone, while itis about 2400 m in the platform of the Tazhong uplift. In consid-eration of the regional extensional setting and no depositionalhiatus or erosion in the CambrianeEarly Ordovician period, it

Figure 7. Seismic profile across the Middle Tazhong Uplift showing fault and stratigraphy inare in their color definitions: CambrianeEarly Ordovician in green, Late Ordovician in red, Scyan. The tops in the profiles are calibrated by the well log data and the representative strataTop of the Devonian System; Tg5: Top of the late Ordovican Sangtamu Formation; Tg51: TopFormation; Tg6: Top of the Cambrian System; Tg61: Top of the Middle Cambrian Awatage Forreferred to the web version of this article.)

should be reasonable that the extensional fault controlled thethickness differences across the Tazhong No. 1 fault belt. In theother profiles in the middle-western of Tazhong uplift, such asprofiles AeA0 , BeB0, CeC0 (Figs. 6e9), the Cambrianeearly Ordovi-cian extensional faults are visible but that their throws are rela-tively minor.

4.2. Thrust faulting in the Late Ordovician

Eighteen Late Ordovician fault strands have been recognizedand the faults present in subparallel NW/NNW trending distribu-tion in plan views (Figs. 4 and 6e9 and Table 1). It can be divided

terpretations. See Figure 4: BeB0 for location. Dash lines indicate unconformities; FaultsilurianeDevonian in purple and the faults associated with Permian magmatic plugs inof the seismic sequences can be seen from Figure 3. Tg: Top of the Permian System; Tg3:of the late Ordovican Lianglitage Formation; Tg52: Top of the early Ordovican Yingshanmation. (For interpretation of the references to colour in this figure legend, the reader is

Figure 8. Seismic profile across the Middle Tazhong Uplift showing fault and stratigraphy interpretations. See Figure 4: CeC0 for location. Dash lines indicate unconformities; Faultsare in their color definitions: CambrianeEarly Ordovician in green, Late Ordovician in red, SilurianeDevonian in purple and the faults associated with Permian magmatic plugs incyan. The tops in the profiles are calibrated by the well log data and the representative strata of the seismic sequences can be seen from Figure 3. Tg: Top of the Permian System;Tg3: Top of the Devonian System; Tg5: Top of the late Ordovican Sangtamu Formation; Tg51: Top of the late Ordovican Lianglitage Formation; Tg52: Top of the early OrdovicanYingshan Formation; Tg6: Top of the Cambrian System; Tg61: Top of the Middle Cambrian Awatage Formation. (For interpretation of the references to colour in this figure legend,the reader is referred to the web version of this article.)

C. Li et al. / Marine and Petroleum Geology 39 (2013) 48e5854

into six groups according to their attributes and distribution. Eachgroup is made up of several faults, and they have been named asf1e1, f2e2 and so on (Fig. 4; Table 1). The thrusting deformationdegrees are different along the Tazhong No. 1 fault belt. Theintensity and scale of the faults in the middle and the western arequite small in comparisonwith the eastern, and the differences canbe seen from the fault throws on seismic sections (Figs. 6e9,Table 1).

The structures in the eastern of Tazhong uplift Area are a seriesof arc-shaped overthrust nappes formed in the front of forelandthrust belts in the Late Ordovician (Li et al., 2009). The Tazhong No.1 Fault is a basement-involved thrust characterized by intensethrusting and back thrusting, and the thrusting offset (f1e1) in thestrongest deformation area is over 800 m (Fig. 9, Table 1). Hangingwall strata are folded and a back thrust triangular zone is formedbecause of the barrier of the stable North Tarim block (Fig. 1:location of the North depression). Within the thrust belts, thestructural style are classic compressive structures, including fault-

Figure 9. Seismic profile across the eastern Tazhong Uplift showing fault and stratigraphy inare in their color definitions: CambrianeEarly Ordovician in green, Late Ordovician in red, Scyan. The tops in the profiles are calibrated by the well log data and the representative straTg3: Top of the Devonian System; Tg5: Top of the late Ordovican Sangtamu Formation; TgYingshan Formation; Tg6: Top of the Cambrian System; Tg61: Top of the Middle Cambrian Athe reader is referred to the web version of this article.)

propagation folds (Figs. 4 and 9: f5e1, f6e1, f6e2) and fault-bendfolds (Figs. 2 and 9: f1e1), and also thrusting wedges constrainedby the boundary between the thrusting fault f1e1 and the back-thrusting fault f5e1. Structures in the eastern of Tazhong upliftArea were considered as intra-cratonic structural deformation inprevious studies (Wu et al., 2005; Li et al., 2008), and the forelanddeformation characteristics are recognized in the recent years, thestructural deformation may due to foreland subsidence of the areain the deformational front (Li et al., 2009; Wu et al., 2012). Asshown in Figure 9, most of the northeastward shortening wasabsorbed by a pattern of fault-related folds, and still some of theshortening was absorbed by southwestward directed back thrusts.This fault f5e1 and another fault (f6e1) in Tazhong No. 5 belt thrustin the opposite direction, and a gentle syncline formed between thetwo faults (Fig. 9).

In the middle of Tazhong uplift Area, Tazhong No. 1 Fault (Fig. 8,fault f1e2) shows quite a small thrust displacement. There area series of back-thrust faults nearly parallel to Tazhong No. 1 Fault

terpretations. See Figure 4: DeD0 for location. Dash lines indicate unconformities; Faultsilurian-Devonian in purple and the faults associated with Permian magmatic plugs inta of the seismic sequences can be seen from Figure 3. Tg: Top of the Permian System;51: Top of the late Ordovican Lianglitage Formation; Tg52: Top of the early Ordovicanwatage Formation. (For interpretation of the references to colour in this figure legend,

Figu

re10

.Strike

profi

leacross

theTa

zhon

gUplift

andon

esh

owingfaultan

dstratigrap

hyinterpretation

s.Se

eFigu

re4:

EeE0

forlocation

.Dashlin

esindicate

unco

nformities;

Faults

arein

theirco

lorde

finition

s:Ca

mbriane

Early

Ordov

icianin

gree

n,Late

Ordov

icianin

red,

Silurian

eDev

onianin

purple

andthefaults

associated

withPe

rmianmag

matic

plug

sin

cyan

.The

tops

intheprofi

lesarecalib

ratedby

thewelllog

data

andtherepresen

tative

strata

ofthe

seismic

sequ

encescanbe

seen

from

Figu

re3.

Tg:To

pof

thePe

rmianSy

stem

;Tg

3:To

pof

theDev

onianSy

stem

;Tg

5:To

pof

thelate

Ordov

ican

Sang

tamuFo

rmation;

Tg51

:To

pof

thelate

Ordov

ican

Lian

glitag

eFo

rmation;

Tg52

:To

pof

theea

rlyOrdov

ican

Ying

shan

Form

ation;

Tg6:

Topof

theCa

mbrianSy

stem

;Tg

61:To

pof

theMiddleCa

mbrianAwatag

eFo

rmation.

(For

interpretation

ofthereferenc

esto

colour

inthis

figu

relege

nd,the

read

eris

referred

totheweb

versionof

this

article.)

C. Li et al. / Marine and Petroleum Geology 39 (2013) 48e58 55

(Fig. 4: f3e2, f3e3, f3e4), and some present flower structures suchas in the Central Fault belt and Tazhong No. 10 Belt (Figs. 7 and 8).The Central Fault Belt is a pop-up structure and controlled by twocounter-thrusting faults (Fig. 4). The strata are heavily denuded inthe Central Fault belt, resulting in a direct contact between theCarboniferous and the Lower Ordovician. In comparison with theeast, the deformation of Tazhong No. 10 Belt is weak and presentsa typical asymmetric fold with a south-steep and north-gentleconfiguration in seismic profiles (Figs. 7 and 8).

In western of Tazhong uplift Area, especially among Well GroupTazhong 45, Tazhong No.1 Fault shows basement-involved features(Fig. 6: f1e3 and Table 1), and its offsets are relatively small,generally less than 200 m. In comparison with the eastern portion,the tectonic intensity is quite weak, and the thrust fault is gentlydipping.

4.3. Strike-slip faulting in the SilurianeDevonian

As stated above, the tectonic activities were intense in theSilurianeDevonian (Jia, 1997; Li et al., 2004, 2009). The Tazhonguplift may have been uplifted as a whole resulted from the violentthrusting in the southeast Tarim block in the Middle Devonian (Jia,1997; Wu et al., 2012). Influenced by the NE trending basement andthe pre-existed faults, a series of the strike-slip faulting developedin the north slop of the Tazhong uplift Area (Li et al., 2008).

Faulting in the SilurianeDevonian is a series of NNE strike-slipfaults spreading northeastwards under the background of trans-pressional stress regime. Eighteen groups of faults were recognizedon the 3-D seismic data (Figs. 4a, 10, and Table 2). The fault can alsobe well manifested in the coherent map of the well group Tazhong45 inwestern of Tazhong uplift Area (Fig. 4b). Most of the strike-slipfault zones are made up of three parts, that is, a main fault,subordinate en echelon faults, and fault troughs. The main faultsare steeply dipping, even vertical, on seismic profiles (Fig. 10). Theypropagate upwards from the basement, and terminate at the baseof the Carboniferous strata (Tg3), and present positive flowerstructures (e.g., Fig. 10:N12) or negative structures (e.g., Fig. 10:N5and N6) on seismic profiles. Though the vertical offsets are quitesmall, the lateral effects can reach as far as several hundred metersto either side. The subordinate en echelon faults generally splaytoward the northeast. They appear on seismic profiles as apparentnormal faults with a NNE strike and extend a short distance inlaterally (Figs. 4a, b and 10). The fault troughs are associated withthe main faults and are often rhombic in plan (Fig. 4a). Their northand south boundaries are controlled by multi-branched faults(Fig. 4a, b).

4.4. Faulting associated with Permian magmatic plugs

The Permian magmatic rocks are widely distributed in thewhole Tarim Basin (Chen et al., 1997, 2006; Yang et al., 2005; Liuet al., 2011; Yu et al., 2009; Pu et al., 2011). Chen et al. (1997,2006) have discussed the distribution from the outcrop, drillingwells and aeromagnetics anomaly.

In Tazhong uplift Area, the Permian igneous rocks widelyoccurred in the middle and the western, especially in the wellTazhong 45 zone, and they have random seismic reflection char-acteristics. As shown in Figure 10, magmatic plugs have beeninterpreted to be preferentially distributed along pre-existingfaults, particularly along the SilurianeDevonian strike-slip faults.To recognize them from the SilurianeDevonian faults is that theycut off the more strata till the top of Permian (Tg) (Fig. 10: cyanfault). Seen from the seismic section Figure 10, the attitudes offaults are in high-angle almost in vertical, and its influence ranges is

Table 1Late Ordovician fault elements of Tazhong Uplift.

Name Characteristics Styles Attitude (strike) Length (km) Forming time Displacement (m) Representative sections

f1e1 Basement involved Thrust NW 71.8 O3 800 Figure 9 DeD0

f1e2 Basement involved Thrust NW 103.7 O3 150 Figure 8 CeC0

f1e3 Basement involved Thrust NW 31 O3 240 Figure 6 AeA0

f2e1 Cover-decollement Thrust NW 16 O3 30f2e2 Cover-decollement Thrust NW 59.5 O3 45f2e3 Basement involved Thrust NW 17 O3 100 Figure 7 BeB0

f3e1 Cover-decollement Thrust NNW 12 O3 60f3e2 Cover-decollement Thrust NW 46.6 O3 300 Figure 8 CeC0

f3e3 Cover-decollement Thrust NNW 26 O3 200 Figure 8 CeC0

f3e4 Cover-decollement Thrust NW/NWW 25.3 O3 120f4e1 Basement involved Thrust NNW 18 O3 300f4e2 Basement involved Thrust NW 25.3 O3 400f5e1 Cover-decollement Thrust NW 55.2 O3 120 Figure 9 DeD0

f5e2 Cover-decollement Thrust EW 9 O3 400f6e1 Basement involved Thrust EW 34.5 O3 400 Figure 9 DeD0

f6e2 Cover-decollement Thrust EW 13 O3 100 Figure 9 DeD0

C. Li et al. / Marine and Petroleum Geology 39 (2013) 48e5856

a relative small scale in space. In plan view, they appear to bea spotty or bandy distribution (Fig. 4: cyan fault).

5. Effect of the faulting systems on the hydrocarbonaccumulation

The Paleozoic faulting systems in Tazhong uplift play importantroles on the hydrocarbon accumulation. They have not onlyreconstructed the existed low-porosity and low-permeabilityreservoirs but also controlled the distribution of the high-qualityreservoirs resulted from their structural differentiations (Wuet al., 2010a, 2012). The four phases faulting systems have playeddifferent roles on the hydrocarbon accumulation in Tazhong upliftArea.

5.1. The north-south zoning of the hydrocarbon accumulation bythe extensional CambrianeEarly Ordovician faulting

Weak zones formed during the CambrianeEarly Ordovicianextensional faulting influence subsequent tectonic movements.They set the border between the Tazhong Uplift and the ManjiaerDepression. As a result, the Tazhong uplift develops along thelocation of the CambrianeEarly Ordovician fault. The subparalleledTazhong No. 1 fault belt, central fault belt and Tazhong No. 10 beltdevelop in theMiddle Ordovician (Fig. 4), and form the south-northzoning structural framework in Tazhong Uplift.

Influenced by the zoning characteristics, the hydrocarbondistribution in the Tazhong Uplift varies across the Tazhong No. 10

Table 2The SilurianeDevonian fault elements of Tazhong Uplift.

Name Characteristics Styles Attitude (strike) Length (km)

N1 Transtensional Slip NNE 22.2N2 Transpressional Slip NE 21N3 Transtensional Slip NE Over the 3DN4 Transtensional Slip NE 12N5 Transtensional Slip NNE 20.5N6 Transtensional Slip NE 18N7 Transpressional Slip NE Over the 3DN8 Transtensional Slip NE Over the 3DN9 Transpressional Slip NE 31N10 Transtensional Slip NE 17N11 Transtensional Slip NE Over the 3DN12 Transpressional Slip NE Over the 3DN13 Transtensional Slip NE 14N14 Transtensional Slip NE 12N15 Transtensional Slip NE 9

belt. The karst reservoir is well developed in the north side becauseof its flat slope and sufficient water leaching. On the contrary, thekarstification of the south side is relatively poor for the existence ofa steep slope. The hydrocarbon migration and accumulation arecontrolled by the zonation of structure and reservoir which makesthe north of the Tazhong Uplift a petroleum enriched area.

5.2. The forming and distribution of the structural traps affected bythe late Ordovician faulting

In late Ordovician, the eastern of the Tazhong uplift experiencedintense uplift and formed large erosion unconformities. The centralfault belt and the Tazhong No.10 belt were reactivated, and the NWtrending thrusts come into finalization in this period. The NWtrending faults not only controlled the structural framework ofnorth-south zoning, but also the distribution of the structural traps.For the forming of the Tazhong uplift, the Tazhong No. 1 belt, Taz-hong No. 10 belt and the Central fault belt developed, accompa-nying the development of a large number of CambrianeOrdovicianstructural traps. In the lower Paleozoic, the Tazhong uplift wasfirstly a huge unified anticlinal trap, and became complication bythe multi-stage modification and adjustment during the middleelate Ordovician period. The modifications caused the destructionof the most CambrianeOrdovician traps, and the long term tiltingof the eastward uplifting caused the decreasing of the traps in thecentral fault belt and the Tazhong No. 10 belt.

The overlying strata of the paleo-uplift are mainly stratigraphictraps, and the development of the Tazhong uplift controlled the

Forming time Displacement (m) Representative sections

SeD 100 Figure 10 EeE0

SeD 60 Figure 10 EeE0

area SeD 40 Figure 10 EeE0

SeD 100 Figure 10 EeE0

SeD 200 Figure 10 EeE0

SeD 40 Figure 10 EeE0

area SeD 100 Figure 10 EeE0

area SeD 60 Figure 10 EeE0

SeD 40 Figure 10 EeE0

SeD 200 Figure 10 EeE0

area SeD 100 Figure 10 EeE0

area SeD 100 Figure 10 EeE0

SeD 200 Figure 10 EeE0

SeD 60 Figure 10 EeE0

SeD 60 Figure 10 EeE0

C. Li et al. / Marine and Petroleum Geology 39 (2013) 48e58 57

forming and distribution of the stratigraphic traps. The overlyingstrata are more apt to form non-structural traps and most non-structural traps developed around the slope of the paleo-uplift.

5.3. The east-west zonality of the hydrocarbon enrichment affectedby the NNE SilurianeDevonian faulting

The NNE SilurianeDevonian strike-slip faulting has divided theTazhong uplift into several zones, and resulted in zonation of thehydrocarbon distribution from east to west. The oil and gas trapsidentified in the western Tazhong uplift Area in the last few yearswere mostly distributed along the strike-slip faults, such as theWell Tazhong 4 reservoir, the Well Tazhong 45 reservoir and theWell Tazhong 10 reservoir.

The SilurianeDevonian strike-slip faulting can destroy the pre-existed reservoirs and be channels for the late hydrocarbonmigration and accumulation. The late Silurianmay be amain periodof hydrocarbon filling period (Wu et al., 2012), andmany large scalepaleo-reservoirs formed in this time. The NNE SilurianeDevonianstrike-slip faults cut through the paleo-reservoir, and are the majorchannels that the surface water penetrates and washes the paleo-reservoir. Most reservoirs were destroyed and the asphalt sand-stone developed in this period in Tazhong uplift Area (Zhang andZhao, 2004; Guo and Chen, 2006; Wang et al., 2009).

The zonality of strike-slip fault caused the difference of thedeveloping, types and forming time of the karstification in differentzones. The deep hydrothermal fluid, the acid water carried by thehydrocarbon migration, and the basin compaction fluid in theburial stage are apt to corrosion along the deep slip faults and theirfracture systems. The high production gas/oil wells with high-quality reservoir in the western Tazhong uplift Area, such as theTazhong 45 and Tazhong 44, experienced well buried karstification.At the same time, the slip belts are the favorable area of the fracturedevelopment.

5.4. The SeC reservoir impacted by the Permian faulting

The faulting associated with Permian magmatic plugs impactedthe late SilurianeCarboniferous (SeC) reservoir. The faults runthrough the deep Ordovician source rocks and provide access forhydrocarbon migration to the SeC reservoir. The hydrocarbon canmigrate vertically along the igneous dikes, igneous pillars or theigneous fractures. The well 47 in the western Tazhong uplift Areaobtained industrial oil flow in Silurian and Carboniferous, whichindicates a new field for hydrocarbon exploration in igneousreservoir. Large scale fractures developed in the Permian igneous inthe western Tazhong uplift Area, which can improve the reservoireffectively. Besides the well 47, well 45 and Tazhong 23 also gainedindustrial oil or gas flow, which present a good prospect to findigneous reservoir in Tazhong uplift Area. But the failure of the well63, which drilled 7 m dolerite, also indicates the complexity of theigneous reservoir.

6. Conclusions

With above analysis and discussion, some conclusions aredrawn as follows.

1. There were four stages of Paleozoic faulting in Tazhong upliftArea, that is, extensional faulting in the CambrianeEarlyOrdovician, NW trending thrusting in the Late Ordovician,northeastward strike-slip faulting in the SilurianeDevonianand faulting associated with Permian magmatic plugs,respectively.

2. Extensional faulting in the CambrianeEarly Ordovician laid thefoundation for subsequent tectonic movements. The LateOrdovician faults were intense thrusting in the eastern alongTazhong No. 1 Fault, relatively gentle thrusting in the middleand the western. SilurianeDevonian strike-slip faults trend tothe northeast, and consist of three components: main andsubordinate en echelon faults, and fault troughs. Permianmagmatic plugs are generally associated with pre-existingfaults.

3. The fault systems influenced the hydrocarbon accumulationand enrichment. The extensional CambrianeEarly Ordovicianfaulting controlled the zonation of the hydrocarbon accumu-lation; the Late Ordovician northwest faulting affected theforming of the structural traps and hydrocarbon enrichment;The NNE SilurianeDevonian strike-slip faulting divided theTazhong uplift into several zones and destroyed the early traps;and the faulting associated with Permian magmatic plugsinfluenced the Silurian-Carboniferous reservoir.

Acknowledgments

This study is financially supported by National Natural ScienceFoundation of China (Grant No. 412021471), the National BasicResearch Program of China (No. 2011CB201100), National KeyScience and Technology Planning Project (No. 2011ZX05002-002).We acknowledge the guidance of Professor Jia Chengzao, acade-mician of Chinese Academy of Sciences, Research Institute ofPetroleum Exploration, CNPC. And we also thank Senior EngineerYang Haijun andHan Jianfa, TarimOil Company, CNPC, for their helpand support in using the seismic data andwell data. We are gratefulto Dr. Thomas Hadlari and the other anonymous reviewers for theircomments in improving the manuscript.

References

Allen, M.B., Windley, B.F., Zhang, C., 1992. Paleozoic collisional tectonics and mag-matism of the Chinese Tian Shan, Central Asia. Tectonophysics 220, 89e115.

Chen, H.L., Yang, S.F., Dong, C.W., Jia, C.Z., Wei, G.Q., Wang, Z.G., 1997. Confirmationof Permian basite zone in Tairm basin and its tectonic significance. Geochimica26 (6), 77e87 (in Chinese with English abstract).

Chen, H.L., Yang, S.F., Wang, Q.H., Luo, J.C., Jia, C.Z., Wei, G.Q., Li, Z.L., He, G.Y., Hu, A.P.,2006. Sedimentary response to the EarlyeMid Permian basaltic magmatism inthe Tarim plate. Geology in China 33 (3), 545e551 (in Chinese with Englishabstract).

Gao, J., Long, L.L., Klemd, R., Qian, Q., Liu, D.Y., Xiong, X.M., Su, W., Liu, W., Wang, Y.T.,Yang, F.Q., 2009. Tectonic evolution of the South Tianshan orogen and adjacentregions, NW China: geochemical and age constraints of granitoid rocks. Inter-national Journal of Earth Sciences 98, 1221e1238.

Guo, J.J., Chen, J.F., 2006. Geologic feature and study progress of Silurian asphalticsandstone in Tazhong Area, Tarim basin. Xinjiang Petroleum Geology 27 (2),151e155 (in Chinese with English abstract).

He, D.F., Jia, C.Z., Zhou, X.Y., Shi, X., Wang, Z.M., Pi, X.J., Zhang, C.J., 2005. Controlprinciples of structures and tectonics over hydrocarbon accumulation anddistribution in multi-stage superimposed basins. Acta Petrolei Sinica 26 (3), 1e9(in Chinese with English abstract).

Jia, C.Z., Wei, G.Q., Yao, H.J., Li, L.C., 1995. The Tectonic Evolution and RegionalTectonic. Petroleum Industry Press, Tarim basin. Beijing, pp. 1e215 (in Chinesewith English abstract).

Jia, C.Z., 1997. The Tectonic Characteristics and Petroleum. Petroleum Industry Press,Tarim basin, China. Beijing, pp. 1e110 (in Chinese with English abstract).

Li, B.L., Guan, S.W., Li, C.X., Wu, G.H., Yang, H.J., Han, J.F., Luo, C.S., Miao, J.J., 2009.Paleo-tectonic evolution and deformation features of the lower uplift in thecentral Tarim basin. Geological Review 55 (4), 521e530 (in Chinese with Englishabstract).

Li, C.X., Jia, C.Z., Li, B.L., Yang, G., Yang, H.J., Luo, C.S., Han, J.F., Wang, X.F., 2009.Distribution and tectonic evolution of the Paleozoic fault system, the northslope of Tazhong Uplift, Tarim basin. Acta Geological Sinica 83 (8), 1065e1073(in Chinese with English abstract).

Li, C.X., Wang, X.F., Li, B.L., 2010. Paleozoic faulting structure styles of the TazhongLow Uplift, Tarim basin and its mechanism. Acta Geological Sinica 84 (12),1727e1734 (in Chinese with English abstract).

Li, D.S., Liang, D.G., Jia, C.Z., Wang, G., Wu, Q.Z., He, D.F., 1996. Hydrocarbon accu-mulation in the Tarim Basin, China. AAPG Bulletin 80 (10), 1587e1603.

C. Li et al. / Marine and Petroleum Geology 39 (2013) 48e5858

Li, M.J., Hu, S.H., Wang, Q.G., Li, X.Z., Chen, J., 2006. Discovery of strike-slip faultsystem in Tazhong area and geologic meaning. Oil Geophysical Prospecting 41(1), 116e121 (in Chinese with English abstract).

Li, M.J., Zheng, M.L., Feng, C.R., Zhang, J.Y., 2004. Structural characteristics andevolution of Tazhong low uplift. Journalof Xi’an Shiyou University (NaturalScience Edition) 19, 43e45 (in Chinese with English abstract).

Li, Y.J., Wu, G.Y., Meng, Q.L., Yang, H.J., Han, J.F., Li, X.S., Dong, L.S., 2008. Faultsystems in central area of the Tarim basin: geometry, kinematics and dynamicsettings. Chinese Journal of Geology 43 (1), 82e118 (in Chinese with Englishabstract).

Lin, C.S., Yang, H.J., Liu, J.Y., Cai, Z.Z., Peng, L., Xiao, X.F., Yang, Y.H., 2008. Paleoupliftgeomorphology and paleogeographic framework and their controls on theformation and distribution of stratigraphic traps in the Tarim Basin. Oil & GasGeology 29 (2), 189e197 (in Chinese with English abstract).

Lin, C.S., Yang, H.J., Liu, J.Y., Peng, L., Cai, Z.Z., Yang, X.F., Yang, Y.H., 2009. Paleo-structural geomorphology of the Paleozoic central uplift belt and its constrainton the development of depositional facies in the Tarim Basin. Science in ChinaSeries D: Earth Sciences 52 (6), 823e834.

Lin, C.S., Yang, H.J., Liu, J.Y., Rui, Z.F., Cai, Z.Z., Zhu, Y.F., 2012. Distribution and erosionof the Paleozoic tectonic unconformities in the Tarim Basin, Northwest China:significance for the evolution of paleo-uplifts and tectonic geography duringdeformation. Journal of Asian Earth Sciences 46, 1e19.

Liu, X., Guan, P., Pan, W.Q., Tian, W., Huang, S.Y., Pan, Y., Jing, B., Yu, H.J., 2011.Meticulous characterization of Permian volcanic rocks’ spatial distributionand its geological significance in the Tarim Basin. Acta Scientiarum Natu-ralium Universitatis Pekinensis 47 (2), 315e320 (in Chinese with Englishabstract).

Lu, X.X., Hu, X., 1997. Hydrocarbon accumulation and distribution in Tazhong LowUplift of Tarim basin. Oil & Gas Geology 18 (4), 288e293 (in Chinese withEnglish abstract).

Luo, J.H., Zhou, X.Y., Qiu, B., 2005. Petroleum geology and geological evolution of theTarimeKarakum and adjacent areas. Geological Review 51 (4), 409e415.

Mattern, F., Schneider,W., 2000. Suturing of the Proto- and Paleo-Tethys oceans in thewestern Kunlun (Xinjiang, China). Journal of Asian Earth Sciences 18, 637e650.

Nakajima, T., Maruyama, S., Uchiumi, S., Liou, J.G., Wang, X.Z., Xiao, X.C.,Graham, S.A., 1990. Evidence for Late Proterozoic subduction from 700-Myr-oldblueschists in China. Nature 346, 226e263.

Pu, R.H., Dang, X.H., Xu, J., Guo, Q., Yi, H.J., 2011. Permian division and correlationand distribution of volcanic rocks of Tarim basin. Acta Petrologica Sinica 27 (1),166e180 (in Chinese with English abstract).

Shaw, J.H., Connors, C.D., Suppe, J., 2005. Seismic Interpretation of ContractionalFault-related Folds. In: An AAPG Seismic Atlas, Studies in Geology[C], vol. 53.AAPG, Tulsa, OK, pp. 1e156.

Sun, L.D., Li, Y.J., Jiang, T.W., Yang, H.J., 2007. The central Tarim lower uplift:a composite hydrocarbon accumulation play in the Tarim basin, NW China.Chinese Journal of Geology 42 (3), 602e620 (in Chinese with English abstract).

Suppe, J., 1983. Geometry and kinematics of fault-bend folding. American Journal ofScience 283 (3), 684e721.

Wang, F., Wang, B., Shu, L.S., 2010. Continental tholeiitic basalt of the Akesu area(NW China) and its implication for the Neoproterozoic rifting in the northernTarim. Acta Petrologica Sinica 26 (2), 547e558 (in Chinese with Englishabstract).

Wang, Q.H., Tang, Z.J., Zhao, F.Y., Zhu, Y.F., Li, H., 2009. Petroleum accumulationgeologic condition and explorative prospect of Silurian in Tarim Basin. XinjiangPetroleum Geology 30 (2), 168e170 (in Chinese with English abstract).

Wang, Z.H., 2004. Tectonic evolution of the western Kunlun orogenic belt, westernChina. Journal of Asian Earth Science 24 (2), 153e161.

Wei, G.Q., Jia, C.Z., Li, B.L., 2002. Periphera foreland basin of Silurian to Devonian inthe South of Tarim Basin. Chinese Science Bulletin 47 (Suppl.), 44e48 (inChinese with English abstract).

Wu, G.H., Ju, Y., Yang, C., Zhao, K.Z., 2010a. Tectonic controlling fators of Ordovicianreef and bank reservoir in Tazhong Uplift in Tarim basin. Xinjiang PeroleumGeology 31 (5), 467e470 (in Chinese with English abstract).

Wu, G.H., Li, Q.M., Xiao, Z.Y., Li, H.H., Zhang, L.P., Zhang, X.J., 2009. The evolutioncharacteristics of palaeo-uplifts in Tarim basin and its exploration directions foroil and gas. Geotectonica et Metallogenia 33 (1), 124e130 (in Chinese withEnglish abstract).

Wu, G.L., Li, Q.M., Zhang, B.S., Dong, L.S., Zhang, G.Y., Zhang, H.Q., 2005. Structuralcharacteristics and exploration fields of No. 1 Faulted Slope Break in Tazhongarea. Acta Petrolei Sinica 26 (1), 27e30 (in Chinese with English abstract).

Wu, G.H., Sun, J.H., Guo, Q.Y., Tang, T., Chen, Z.Y., Feng, X.J., 2010b. The distribution ofdetrital zircon UePb ages and its significance to Precambrian basement inTarim Basin. Acta Geoscientica Sinica 31 (1), 64e72 (in Chinese with abstract).

Wu, G.H., Yang, H.J., Qu, T.L., Li, H.W., Luo, C.S., Li, B.L., 2012. The fault systemCharateristics and its controlling roles on marine hydrocarbon in the Centraluplift, Tarim basin. Acta Petrologica Sinica 028 (3), 793e804 (in Chinese withabstract).

Xiao, W.J., Windley, B.F., Liu, D.Y., Jian, P., Liu, C.Z., Yuan, C., Sun, M., 2005. Accre-tionary tectonics of the Western Kunlun Orogen, China: a PaleozoiceearlyMesozoic, long-lived active continental margin with implications for thegrowth of southern Eurasia. Journal of Geology 113 (6), 687e705.

Xu, B., Jian, P., Zheng, H.F., Zou, H.B., Zhang, L.F., Liu, D.Y., 2005. UePb zircongeochronology and geochemistry of Neoproterozoic volcanic rocks in the TarimBlock of northwest China: implications for the breakup of Rodinia superconti-nent and Neoproterozoic glaciations. Precambrian Research 136, 107e123.

Xu, B., Xiao, S.H., Zou, H.B., Chen, Y., Li, Z.X., Song, B., Liu, D.Y., Zhou, C.M., Yuan, X.L.,2009. SHRIMP zircon UePb age constraints on Neoproterozoic Quruqtaghdiamictites in NW China. Precambrian Research 168, 247e258.

Yang, S.F., Chen, H.L., Ji, D.W., Li, Z.L., Dong, C.W., Jia, C.Z., Wei, G.Q., 2005. Geologicalprocess of early to middle Permian Magmatism in Tarim Basin and its geo-dynamic significance. Geological Journal of China Universities 11 (4), 504e511(in Chinese with English abstract).

Yu, X., Chen, H.L., Yang, S.F., Li, Z.L., Wang, Q.H., Li, Z.H., 2009. Geochemical featuresof Permian basalts in Tarim basin and compared with Emeishan LIP. Acta Pet-rologica Sinica 25 (6), 1492e1498 (in Chinese with English abstract).

Zhang, C.L., Li, Z.X., Li, X.H., Ye, H.M., 2009. Neoproterozoic mafic dyke swarms atthe northern margin of the Tarim Block, NW China: age, geochemistry, petro-genesis and tectonic implications. Journal of Asian Earth Sciences 35, 167e179.

Zhang,C.L., Yang,D.S.,Wang,H.Y.,Dong,Y.G.,Ye,H.M., 2010.Neoproterozoicmaficdykesand basalts in the Southern Margin of Tarim, Northwest China: age, geochemistryand geodynamic implications. Acta Geologica Sinica 84 (3), 549e562.

Zhang, L.C., Li, Z.C., Li, X.H., Yu, H.F., Ye, H.M., 2007. An early Paleoproterozoic high-Kintrusive complex in southwestern Tarim Block, NW China: age, geochemistry,and tectonic implications. Gondwana Research 12, 101e112.

Zhang, X.B., Zhao, X.K., 2004. Relationship between Tazhong tectonic evolution andSilurian hydrocarbon distribution in Tarim basin. Natural Gas Exploraiton &Development 27 (2), 11e16 (in Chinese with English abstract).

Zhao, Z.J., Zhou, X.Y., Fan, G.Z., 2006. Dominant forming stages of structural traps inTazhong area, Tarim basin: distribution and implication for hydrocarbonaccumulation. Marine Origin Petroleum Geology 11 (2), 1e8 (in Chinese withEnglish abstract).

Zhang, Z.M., Jia, C.Z., 1997. Palaeohighs in craton basin of Talimu and the explorationobjectives. Journalof Xi’an Shiyou University (Natural Science Edition) 12 (3),8e13 (in Chinese with English abstract).

Zhang, Z.S., Li, M.J., Liu, S.P., 2002. Generation and evolution of Tazhong low uplift.Petroleum Exploration and Development 29 (1), 28e31 (in Chinese withEnglish abstract).

Zhou, X.Y., Li, B.L., Chen, Z.X., Yu, H.F., Jing, B., 2011. The tectonic genesis andexploration targets of large oilegas fields in Tazhong area, Tarim basin. XinjiangPetroleum Geology 32 (6), 211e217 (in Chinese with English abstract).