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GSA Bulletin; February 2002; v. 114; no. 2; p. 131–152; 19 figures.

Permian sedimentary record of the Turpan-Hami basin and adjacentregions, northwest China: Constraints on postamalgamation

tectonic evolution

Marwan A. Wartes*Alan R. CarrollDepartment of Geology and Geophysics, University of Wisconsin, Madison, Wisconsin 53706, USA

Todd J. GreeneDepartment of Geological and Environmental Sciences, Stanford University, Palo Alto, California 94305-2115, USA

ABSTRACT

The Permian marks an important, yetpoorly understood, tectonic transition inthe Tian Shan region of northwestern Chi-na between Devonian–Carboniferous con-tinental amalgamation and recurrent Me-sozoic–Cenozoic intracontinental orogenicreactivation. The Turpan-Hami basin ac-commodated up to 3000 m of sediment andis ideally positioned to provide constraintson this transition. New stratigraphic dataand mapping indicate that extension dom-inated Early Permian tectonics in the re-gion, whereas flexural, foreland subsidencecontrolled Late Permian basin evolution.

Lower Permian strata in the northwest-ern Turpan-Hami basin consist of coarse-grained debris-flow and alluvial-fan depos-its interbedded with mafic to intermediatevolcanic sills and flows. In contrast, LowerPermian rocks in the north-central andnortheastern Turpan-Hami basin uncon-formably overlie a Late Carboniferous vol-canic arc sequence. These Lower Permianstrata include possible shallow-marine car-bonate rocks and thick volcanic and vol-caniclastic rocks that are in turn overlainby littoral- to profundal-lacustrine facies.Above a regional Lower Permian/UpperPermian unconformity, regional sedimen-tation patterns record the development of amore integrated sedimentary basin. TheUpper Permian is entirely nonmarine andcan be correlated east-west along the de-positional strike of the basin. The lower Up-per Permian consists of a broad belt of

*E-mail: [email protected].

braided fluvial deposits shed northward.These strata are overlain by fluctuating lit-toral- and profundal-lacustrine facies andassociated fluvial facies. The uppermostPermian is characterized by shallow lake-plain and fluvial environments.

The Early Permian association of diffusevolcanism and partitioning of subbasins bynormal faulting is consistent with an earlyphase of lithospheric extension. Local rela-tionships indicate west-east extension in theTurpan-Hami basin along faults orientednormal to Late Devonian–Carboniferouscollisional sutures within the Tian Shan.The cause of extension in the wake of Car-boniferous orogenesis remains enigmatic.However, the temporal and spatial relation-ships of the two strain regimes suggest thatthey are genetically related. Upper Permianstratigraphy and unconformities and localLate Permian–Triassic contractional defor-mation record foreland-basin developmentwhen the Turpan-Hami region became awedge-top basin with respect to the northTian Shan fold-and-thrust belt. Flexurallyinduced Late Permian subsidence is alsomanifested in the larger Junggar basin tothe north, where .4000 m of strata are pre-served in the foredeep region. The Turpan-Hami and Junggar basins were deposition-ally connected for much of the LatePermian when a vast lacustrine system de-veloped across northwestern China. Thislacustrine paleogeography was only occa-sionally interrupted, possibly by structuraldamming during uplift of the orogenicwedge.

Keywords: Asia, Junggar basin, lacustrine,stratigraphy, Tian Shan, Xinjiang.

INTRODUCTION

The tectonic assembly of central Asia oc-curred during a series of middle to late Paleo-zoic accretionary events along the southernmargin of the Angara craton (e.g., Coleman,1989; Wang et al., 1990; Windley et al., 1990;Zonenshain et al., 1990; Allen et al., 1993a;Sengor et al., 1993; Carroll et al., 1995; Gaoet al., 1998). However, the remote interior ofAsia remains one of the least understood geo-logic provinces on Earth, and many of the crit-ical details of this complex amalgamation oftectonic elements (i.e., timing, suture zones,subduction polarity, etc.) remain poorlydetermined.

The Permian Period is of particular interestbecause it spans a critical transition betweencontinental amalgamation during the Devoni-an–Carboniferous (e.g., Allen et al., 1993a;Carroll et al., 1995) and the Mesozoic–Ceno-zoic development of intracontinental forelandbasins (e.g., Hendrix et al., 1992). The Perm-ian also records an episode of long-lived (40–50 Ma) basin subsidence, particularly in thesouthern Junggar basin where up to 5 km ofnonmarine strata are preserved (Carroll et al.,1990, 1995). The underlying cause of this tec-tonism continues to be debated, and nearly allpotential end-member tectonic settings havebeen proposed: Extension (Bally et al., 1986;Hsu, 1988; Peng and Zhang, 1989; Allen etal., 1991; Shao et al., 1999), foreland-basinflexure (Xie et al., 1984; Watson et al., 1987;Graham et al., 1990; Carroll et al., 1990,1995), and even regional transtension (Allenet al., 1995; Sengor and Natal’in, 1996). Suchwidely varying interpretations are manifestlythe result of limited field and subsurface data

132 Geological Society of America Bulletin, February 2002

WARTES et al.

Figure 1. Geologic map of northwest China (modified from Chen et al., 1985), illustrating the distribution of Permian outcrops andlocalities discussed in the text.

capable of unequivocally demonstrating thePermian tectonic setting of northwestern Chi-na. Therefore, a detailed understanding of thesedimentary evolution of this region repre-sents an important step toward deconvolvingthe late Paleozoic tectonic regime.

This paper centers on the Permian sedimen-tary record of the Turpan-Hami basin, an east-west elongate depression covering .50 000km2 in the Xinjiang Uygur Autonomous Re-gion, northwestern China (Fig. 1). The Turpan-Hami basin is currently separated from thelarger Junggar basin to the north by the BogdaShan and bound to the south by the northernTian Shan (Fig. 1). We present sedimentologicobservations based on field work spanning.600 km eastward along the strike of thenorthern margin of the Turpan-Hami basin(Fig. 1). The major source of data for our in-terpretations is stratigraphic logs from .30sections of Permian strata. These data allowus to place new constraints on the Permiantectonic evolution of northwestern China.

PERMIAN CHRONOSTRATIGRAPHY

Many intervals of Permian strata in theTurpan-Hami basin are richly fossiliferous.Unfortunately, few detailed biostratigraphicsyntheses have been published in either thewestern or Chinese literature. Chronostrati-graphic studies are limited, particularly innonmarine strata, by floral and faunal ende-mism indicated by the large number of generaand species found only in the Turpan-Hamibasin. Nonetheless, we have assembled a bio-stratigraphic framework that is adequate forthis reconnaissance-level basin analysis (Fig.2).

Lower Permian strata reportedly containage-diagnostic fossils (Fig. 2; Hu Ting, 1998,written commun.), but precise biostratigraphicassignments beyond the epoch-level are prob-lematic. Nonmarine lower Upper Permianstrata contain a diverse assemblage of floraand fauna (e.g., Liao et al., 1987; XPGEG,1991) that aid local correlations such as those

presented in Figure 2. The most precise chron-ostratigraphy within the Turpan-Hami andJunggar basins has been developed for the up-permost Permian and Triassic in response toevaluation of the region’s potential as a non-marine Global Stratotype and Stratotype Point(GSSP) spanning the Permian/Triassic bound-ary (Yang et al., 1986; Cheng and Lucas,1993).

LOWER PERMIANLITHOSTRATIGRAPHY ANDSEDIMENTARY FACIES

Taoxigou Formation

The Lower Permian Taoxigou Formation iswell exposed at Taoshuyuan (TS; Fig. 1) inthe northwestern Turpan-Hami basin and over-lies Upper Carboniferous shallow-marinerocks of the Aoertu Formation (Liao et al.,1987; Carroll et al., 1990, 1995). Here, theTaoxigou Formation is at least 2000 m thickand can be informally divided into lower and

Geological Society of America Bulletin, February 2002 133

PERMIAN SEDIMENTARY RECORD OF TURPAN-HAMI BASIN AND ADJACENT REGIONS, CHINA

Figure 2. Subdivision and correlation of Permian units in the Junggar and Turpan-Hami basins (modified from Zhao, 1982; Chen etal., 1985; Liao et al., 1987; Wartes et al., 2000). Paleontologic data from Zhang (1981), Liao et al. (1987), XPGEG (1991), Cheng et al.(1996), Wu and Zhao (1997), and Hu Ting (1998, written commun.). The Permian series and stages used here conform to those suggestedby Jin et al. (1997) for global chronostratigraphic subdivisions.

upper members on the basis of lithologic dif-ferences (mainly coarse-clastic sedimentaryrocks vs. mainly volcaniclastic rocks; Fig. 3).

DescriptionThe lower member of the Taoxigou For-

mation is characterized by a dominance ofconglomerate lithofacies (Fig. 3). Individualbeds commonly amalgamate into laterallycontinuous sections up to 25 m thick. Bothmatrix- and clast-supported fabrics exist, andmatrix varies from siltstone to coarse-grained

sandstone. Clast sizes range from granule tocobble and are composed of subangular torounded sandstone, limestone, and volcanic li-thologies. Matrix-supported beds grade in-versely from a sharp base characterized bygranule-sized clasts, up through an irregularupper surface marked by protruding cobbles(Fig. 4). Clast-supported fabrics are generallypoorly sorted, massive, and crudely horizon-tally stratified. Plane-bedded and trough cross-stratified sandstone are common and displaytabular and lenticular geometries, respectively.

The uppermost 100 m of the lower TaoxigouFormation consist of moderately organized,trough cross-stratified, clast-supported con-glomerate interbedded with rippled to plane-laminated fine- to medium-grained sandstone.Some of the conglomerate beds fill scours inunderlying thin red mudstone beds.

The upper member of the Taoxigou For-mation is composed predominantly of amal-gamated volcanic beds of mafic to intermedi-ate composition (Fig. 3). These units occur intwo different associations: (1) Aphanitic and


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Figure 3. Measured section of the Lower Permian Taoxigou Formation (P1tx) at Taoshuyuan, northwestern Turpan-Hami basin (seeFig. 1 for location). P1tx1 and P1tx2 refer to informal members discussed in the text. The explanatory legend also applies to othermeasured sections presented throughout this paper.



Figure 4. Debris-flow facies characteristicof the Lower Permian Taoxigou Formationat Taoshuyuan. Stratigraphic up is the topof the photo. Note hammer handle for scale.

porphyritic rocks are commonly separated bythin, fine-grained sandstone and siltstone beds.Subangular, red mudstone clasts are preservedin the lower part of some of these volcanicbeds. Vesicular or amygdaloidal textures arealso observed near the top of this unit. (2)Lesser amounts of aphanitic basalt are char-acterized by irregular upper and lower con-tacts that include mixtures of angular sedi-mentary or volcanic clasts.

InterpretationDeposits of the lower member of the Taox-

igou Formation are interpreted as alluvial fanfacies, dominated by sediment gravity-flowprocesses. The matrix-supported conglomerateexhibits many characteristic features of debrisflows (Fig. 4; Enos, 1977; Gloppen and Steel,1981). The less cohesive, clast-supported con-glomerate lithofacies was deposited via hy-perconcentrated flows (e.g., Smith, 1986;Sohn et al., 1999). Laterally persistent sand-stone beds are interpreted as upper-flow re-gime, unconfined sheetflood deposits, proba-bly laid down during periodic, sediment-chargedflashflood events (e.g., Balance, 1984; Blairand McPherson, 1994). The uppermost 100 mof the lower member of the Taoxigou For-mation is attributed to deposition under morechannelized, fluid-dominated conditions(Miall, 1996). Trough cross-stratification andsome clast imbrication are features consistentwith deposition in longitudinal bars (Rust,1978).

The upper member of the Taoxigou For-mation includes both volcanic flows and sills(Fig. 3). Surface flows are discriminated fromsills primarily on the basis of the mechanical

inclusion of underlying lithologies (rip-upclasts) only along the flow base and the com-mon increase in vesicular to amygdaloidal tex-tures observed near the flow top, recording theupward movement of entrapped gas throughthe denser melt (cf. Ehlers and Blatt, 1982).

Zaobishan Formation

The Lower Permian Zaobishan Formationis best known from a complete, well-exposed330 m section at the type locality Zaobishan(ZB; Fig. 1), where it unconformably overliesthe Carboniferous Liushugou Formation. It isinformally divided into lower, middle, and up-per members on the basis of distinctive lith-ologic features (Fig. 5).

DescriptionThe lower member of the Zaobishan For-

mation is dominated by carbonate and fine-grained siliciclastic lithofacies (Fig. 5). Thebasal contact with the underlying LiushugouFormation is slightly angular (58). The low-ermost 25 cm includes pebble-sized clastssimilar to the underlying andesite and is char-acterized by coarse-grained carbonate grain-stone that includes pisoliths and possibly neo-morphosed fusulinids. The dominantlithofacies in this member are red-yellow ar-gillaceous micrite, interbedded at a 10 cmscale with weakly calcareous red mudstonehaving sparse, micrite-filled burrowing traces.The micrite, as well as lesser, 10–75-cm-thickpackstone and wackestone beds, commonlycontains nodular chert. Several interbeds ofgreen chert up 50 cm thick are also present.

The middle member of the Zaobishan For-mation is composed largely of amalgamatedvesicular basalt and andesite units (Fig. 5).The base of individual beds is commonlysharp and marked by a color change withinthe top of underlying beds.

The lower 25 m of the upper member of theZaobishan Formation consists of cyclically in-terbedded conglomerate and sandy limestone(Fig. 5). Clast-supported conglomerate bedsare tabular to lenticular, 10–30 cm thick, andtypically scoured at their base. Maximum clastsizes (usually ,4 cm) appear at the base ofindividual beds and rapidly fine upward intomedium- to coarse-grained sandstone or fine-grained sandy limestone. Some sandy carbon-ate beds contain low-angle cross-stratificationand fill irregular surfaces such as bedding-toptrough bedforms in conglomerate. Some sharpplanar scours truncate the sandy limestone andare overlain by irregularly spaced granule lay-ers or stringers of mudstone clasts. A series ofcylindrical carbonate structures is encased

within a granule conglomerate and thin sand-stone (Figs. 5 and 6). These structures have adiameter of 60 cm and reach 150 cm in height,with the long axis oriented perpendicular tobedding. Internally, the structures possess acrudely concentric ring fabric in cross section.The remaining 125 m of section is dominatedby dark gray, well-laminated mudstone. Thin(;5 cm) limestone beds are also present,some of which exhibit algal laminations.

InterpretationVariations in carbonate lithofacies (grain-

stone to micrite) record a wide range of en-ergy conditions within the lower member ofthe Zaobishan Formation, which may be eithermarine or lacustrine. Lower Permian marinerocks in the Turpan-Hami basin have recentlybeen confirmed from subsurface samples tothe south via fusulinid identification (fossilidentification by C. Stevens, 1999, writtencommun.). However, in the absence of con-clusive marine fauna, the section at Zaobishanremains enigmatic.

Volcanic beds of the middle member of theZaobishan Formation are interpreted as sur-face flows on the basis of indurated basal con-tacts and vesicular to amygdaloidal texturescommon to modern lava flows (Cashman etal., 1994).

The upper member of the Zaobishan For-mation is interpreted as fluvial and littoral- toprofundal-lacustrine deposits. Lenticular,clast-supported conglomerate deposits recordepisodic, short-lived stream flow based onrapid fining-upward trends, indicative of wan-ing flow. Littoral-lacustrine deposits are char-acterized by mixed carbonate-clastic and sili-ciclastic rocks and include the carbonate towerstructures interpreted as tufas (Fig. 6). Al-though modern tufas form in a wide varietyof environments, they commonly precipitate atsprings along lake margins (e.g., Lowensteinet al., 1999) or even along sublacustrine faults(Scholl, 1960). A relatively rapid deepeningof the lake is suggested by the onset of con-tinuous, mudstone-dominated profundal de-posits (Fig. 5). The presence of millimeter- tosubmillimeter-scale laminations suggests lowsediment flux, dominated by suspension fall-out and anoxic depositional conditions (Keltsand Hsu, 1978; Demaison and Moore, 1980).Modest fluctuations in lake level betweendominantly deep profundal and sublittoral en-vironments are indicated by the periodic de-velopment of thin algal-laminated horizons.

Yierxitu Formation

The Lower Permian Yierxitu Formation isexposed near the village of Tian Shan Xiang


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Figure 5. Measured section of the Lower Permian Zaobishan Formation (P1z) at Zaobishan, north-central Turpan-Hami basin. P1z1,P1z2, and P1z3 refer to informal members discussed in the text (see Fig. 1 for locations and Fig. 3 for legend).



Figure 6. Carbonate tufa tower (field note-book for scale) encased in alluvial-fan gran-ule conglomerate of the upper member ofthe Zaobishan Formation (P1z3).

Figure 7. Measured section of the Lower Permian Yierxitu Formation (P1y) at Tian ShanXiang, northeastern Turpan-Hami basin. P1y1, P1y2, P1y3, and P1y4 refer to informalmembers discussed in the text (see Fig. 1 for locations and Fig. 3 for legend).

in the northeastern Turpan-Hami basin (TSX;Fig. 1). The ;625-m-thick section uncon-formably overlies the Carboniferous Liushu-gou Formation and is divided into four infor-mal members (Figs. 7 and 8A).

DescriptionThe base of the Yierxitu Formation overlies

an undulating, erosional contact with the Liu-shugou Formation. This contact is angular(;58), and the lowest 10 m of section includessubangular to subrounded andesite clasts up to30 cm. The lowermost member of the YierxituFormation is composed of interbedded tuffa-ceous rocks and massive dark gray mudstone(Fig. 7). Tuffaceous beds commonly exhibiterosive bases, are crudely laminated, includeripple and low-angle cross-stratification, andpreserve abundant soft-sediment deformationstructures (Fig. 8B).

The second member of the Yierxitu For-mation is dominated by massive, amalgamatedvolcanic rocks of intermediate composition(Figs. 7 and 8A). Many of the volcanic bedsare aphanitic to cryptocrystalline. Minor ac-cumulations of mudstone and volcaniclasticsandstone are present near the top of themember.

The third member is composed of conglom-erate, sandstone, and mudstone collectivelyrecording a general fining-upward succession(Figs. 7 and 8A). The base of the successionis composed of angular to subangular clast-supported conglomerate beds, 10–50 cmthick, which are scoured at their base and fineupward to massive sandstone and weakly lam-inated siltstone. Mudstone and fine-grainedsandstone, interbedded with the conglomerate,contain broken bivalve fragments, woody de-bris and algal laminations. An interval of silt-stone and thin lens-shaped bodies of mudstone


WARTES et al.

Figure 8. Outcrop photographs of Lower Permian rocks of the Yierxitu Formation at TianShan Xiang. (A) Exposures of volcanic and sedimentary rocks shown in Figure 7. Inter-mediate-composition volcanic rocks of the upper part of P1y2 crop out at the bottom right,overlain by sediments of P1y3 that include the prominent dark bed of profundal-lacustrinemudstone. Volcanic and volcaniclastic rocks of the uppermost member (P1y4) comprisethe remaining Lower Permian section. The saddle along the horizon approximately marksthe Lower Permian/Upper Permian boundary. (B) Low-angle cross-stratification in tuff-aceous facies of the lowermost Yierxitu Formation (P1y1). (C) Large flame structure andassociated soft-sediment deformation at the base of P1y4.

and fine- to medium-grained sandstone over-lies the conglomerate beds. Tabular sandstonebodies containing plant fragments mark themiddle of the fining-upward trend. The bal-ance of the remaining section is dominantlyorganic-rich, submillimeter-scale laminatedmudstone containing disarticulated fish parts,ostracodes, and plant fragments. Several thin(,5 cm), very fine sandstone and siltstonebeds are normally graded and rippled and ex-hibit micro–flame structures at their bases.

The fourth and uppermost member of theYierxitu Formation was only examined in re-connaissance fashion (Figs. 7 and 8A). The

base of the member is a conspicuous bound-ary juxtaposing a thick, tan-colored volcani-clastic sandstone directly upon the laminatedmudstone of the third member. The contact ismarked by convolute lamination, large, upward-tapering flame structures, and mudstone dikesderived from the third member (Fig. 8C). Theoverlying ;200 m of section is not well ex-posed; float indicates that volcanic rocks dom-inate the covered interval. The uppermost 35m of section are composed of a mix of darkgray silty mudstone, green fissile mudstone,medium-grained sandstone, and volcanicrocks. The volcanic lithofacies comprise

weakly stratified, accretionary lapilli, some ofwhich include up to 1 m clasts of vesicularbasalt supported in a tuffaceous matrix.

InterpretationThe basal member of the Yierxitu Forma-

tion is interpreted as subaqueous pyroclasticdeposits. Sedimentary structures indicate rapiddeposition related to unconfined, erosive,high-concentration turbulent flows (e.g.,Chough and Sohn, 1990).

The second member is interpreted as a se-ries of rapidly cooling volcanic flows. The in-tercalation of thin sedimentary beds near thetop indicates that volcanism was not continu-ous and that numerous separate eruptive phas-es are present.

The facies succession within the third mem-ber is interpreted as retrogradational, begin-ning with fan-delta deposition at the base fol-lowed by a gradual lake transgression,culminating in profundal-lacustrine facies. Al-though fan-delta deposits commonly coarsenupward (e.g., Steel et al., 1977), retrograda-tional relationships have been documented inregions where marine transgressions (Maeji-ma, 1988) or lake-level rises (Kazanci, 1988)have ‘‘drowned’’ active alluvial fans. Fan-delta deposits of the Yierxitu Formation areinterpreted on the basis of the low degree ofclast rounding, suggesting limited transport,and the close association of conglomerate withindicators of lacustrine environments (e.g., al-gal laminations and bivalves). Siltstone andsandstone within the middle of this memberare interpreted as a thin, transgressive deltaicsequence (cf. Reading and Collinson, 1996).Lenticular beds, surrounded by mudstone, areinterpreted as small, distal distributary-channel fill in a delta-front setting. Scoured,upward-fining, tabular sandstone beds are in-terpreted as prodelta turbidites, which are, inturn, overlain by finely laminated, profundalmudstone. Normally graded, thin beds of veryfine grained, rippled sandstone and siltstoneare interpreted as distal turbidites.

The base of the fourth member records arapid basinward shift in facies. Similarlyabrupt juxtapositions of basinal lake depositswith thick sandstone bodies have been inter-preted as lowstand deltaic deposits forming af-ter rapid falls in lake level (Scholz et al.,1990). The volcanic rocks overlying the sand-stone appear to be surface flows, similar to thesecond member. The accretionary lapilli withlarge vesicular boulders are attributed toblock-and-ash flows resulting from phreato-magmatic eruptions (e.g., McPhie et al.,1990).



Figure 9. Measured sections of the lowerUpper Permian Daheyen Formation (P2d)along the northern Turpan-Hami basin.Sections are presented from west to east(see Fig. 1 for locations and Fig. 3 forlegend).

UPPER PERMIANLITHOSTRATIGRAPHY ANDSEDIMENTARY FACIES

Daheyen Formation

The lower Upper Permian Daheyen For-mation, as thick as 250 m, was described indetail at three locations along the northernTurpan-Hami basin (Aiweiergou [AR], Tao-donggou [TD], and Zaobishan [ZB]; Figs. 1and 9).

DescriptionIn the northern Turpan-Hami basin, the

Daheyen Formation is separated from under-lying strata by a regional unconformity (Fig.2). This basal surface is well exposed at Tao-donggou (TD) and Zaobishan (ZB) whereconglomerate fills high-relief scours. The Tao-donggou locality is characterized by angularbreccia, containing volcanic clasts up to 70cm, overlying Carboniferous volcanic bedswith an angular discordance of ;208 (Fig.9B). At Zaobishan (ZB), cobble conglomeratedirectly overlies black, laminated lacustrinemudstone of the upper Zaobishan Formation(Fig. 9C). The underlying mudstone becomesincreasingly brown approaching this contact.The dominant lithofacies within the DaheyenFormation is pebble to cobble conglomeratewith a medium- to coarse-grained matrix. AtAiweiergou, the conglomerate is, in part, ma-trix-supported, weakly stratified, and laterallycontinuous (Fig. 9A). More commonly, theconglomerate is moderately to well sorted andexhibits lenticular geometry and a well-organized clast-supported, imbricated fabric.Trough cross-stratification and basal scours upto 1 m in amplitude are abundant. Large silic-ified tree trunks are preserved throughout thesection at Zaobishan. Lesser, fine-grained lith-ofacies at Taodonggou are red to green, mas-sive, ostracode-bearing mudstone. Mudstonebeds also include occasional calcareous nod-ules and rhizoliths. At Aiweiergou, similarmudstone beds overlie angular sandstone andconglomerate breccia.

InterpretationThe basal Daheyen at Taodonggou is inter-

preted as a regolith consisting of material de-


WARTES et al.

rived from the underlying Carboniferous Liu-shugou Formation. The alteration of lacustrinemudstone beneath the unconformity at Zao-bishan represents oxidation during Permiansurface exposure. The limited matrix-support-ed conglomerate is attributed to debris-flowdeposition on the basis of the conglomerate’sfabric and a lack of erosional scouring or in-dicators of tractive transport. The sheet-likedistribution of this lithofacies is consistentwith unconfined flow across alluvial-fan sur-faces (e.g., Blair and McPherson, 1994). Well-organized, clast-supported conglomerate bedsare interpreted as braided fluvial deposits (cf.Miall, 1977; Rust, 1978). Excellent preserva-tion of large trees indicates rapid depositionand burial. The presence of root traces, cal-careous nodules, and brecciation suggest ped-ogenic modification of mudstone lithofaciesduring paleosol development (Retallack,1988). These fine-grained deposits may rep-resent floodplain to palustrine environmentsadjacent to a migrating braided fluvial system.

Tarlong Formation

The lower Upper Permian Tarlong Forma-tion overlies the Daheyen Formation and wasexamined at four localities along the southernBogda Shan (Aiweiergou, Taodonggou, Zao-bishan, and Tian Shan Xiang; Fig. 1).

DescriptionThe base of the Tarlong Formation appears

conformable and is generally defined by a dra-matic decrease in grain size relative to under-lying rocks (Fig. 10). The Tarlong Formationcommonly appears cyclic in outcrop; the for-mation contains repeating packages of mud-stone, sandstone, conglomerate, and a few car-bonate lithofacies (Fig. 11A). The dominantlithofacies is varicolored, massive to laminat-ed, siliciclastic mudstone. Fine- to medium-grained sandstone bodies are well sorted andpossess planar-tabular bedding morphologies,although lens-shaped, trough cross-beddedsandstone bodies with scoured bases are alsopresent. Sandstone beds are commonly char-acterized by sharp bases, many of which infillunderlying mudcracked horizons, and showevidence of burrowing. Many sandstone bedsalso have mud intraclasts and carbonaceousdebris and contain symmetric, asymmetric,and climbing ripples. Conglomerate beds areless common and usually exhibit scoured ba-ses or form distinct channelized bodies (Fig.11B). Thin beds (,20 cm) of massive, micri-tic limestone occur at every locality. Wacke-stone, packstone, and coquina beds exist lo-cally and are the principal fossiliferous facies

containing abundant bivalves, gastropods, os-tracodes, and fish. Algal-laminated facies arealso present at several localities.

InterpretationThe dominant depositional setting inter-

preted for the Tarlong Formation is lake plainto profundal lacustrine. Lake-plain depositsare characterized by mud cracks, interpretedas subaerial-exposure surfaces, and overlyingsheet-like sandstone with horizontal lamina-tion and climbing ripples, indicating upperflow regime and rapid sedimentation (e.g.,Hardie et al., 1978). Periodic fluvial incur-sions across the lake plain are marked by dis-crete, lenticular sandstone and conglomeratebeds bearing carbonaceous debris and mud in-traclasts. Evidence for shallow, littoral-lacustrine deposits include laterally persistent,symmetric wave–rippled sandstone, algal lam-inations, and fossiliferous limestone. Rocks ofthe profundal-lacustrine facies are defined bysubmillimeter-scale laminations and well-preserved fish fossils, indicating a lack of bot-tom-dwelling fauna. Changing lake-shorelineposition is recorded by a cyclic repetition oflithofacies, a feature common to many lakeswith closed-basin hydrology (e.g., Talbot andAllen, 1996). Carroll and Bohacs (1999)named this style of cyclic stratal stacking, the‘‘fluctuating profundal facies association.’’

Lower Cangfanggou Group

The uppermost Permian Lower Cangfang-gou Group is composed of the Quanzijie, Wut-onggou, and Guodikeng Formations (Fig. 2).Measured sections presented here are fromTaodonggou (TD) and Zaobishan (ZB) (Figs.1 and 12).

DescriptionThe Lower Cangfanggou Group is transi-

tional with underlying strata, but is usuallymarked by variegated stratigraphy dominatedby nonlaminated, red, green, and dark gray,siliciclastic mudstone. Amalgamated, lenticu-lar conglomerate and sandstone beds are char-acterized by basal and internal scours, fluteand groove marks, asymmetric ripples andtrough cross-stratification. Many plane-laminated sandstone beds persist laterally fortens of meters and include carbonate mud, pla-nar-tabular cross-bedding, mudstone intra-clasts, and ripples (unidirectional, bidirection-al, and interference). Carbonate facies arecommonly fossiliferous and include tabularsandy micrite, pisolitic and oolitic grainstone,and stromatolites. Gastropods and bivalves areconcentrated in some coquina beds.

InterpretationWe interpret the Lower Cangfanggou Group

paleoenvironments as ephemeral shallowlakes within a fluvial plain. Shallow-lacustrinedeposits are recorded by bidirectional waveripples and oolitic grainstone beds indicatinghigh-energy conditions. Continuous sandstoneand sandy micrite beds are interpreted assheetflood lake-plain deposits on the basis oftheir unconfined geometry, unidirectional cur-rent indicators, and entrained rip-ups of un-derlying mudstone (e.g., Hardie et al., 1978).Fluvial deposits are recognized by their len-ticular morphology, trough cross-stratification,and tool marks at channel bases. These de-posits may represent short-duration fluvial dis-charge because of their abundant upward-fining cycles, suggesting waning flow. Thediversity of fauna indicates a freshwater, well-mixed lake—an interpretation in accord withoxygen isotope studies of this interval (Brandet al., 1993). Similar lithofacies are commonlyobserved in overfilled lake basins with anopen hydrology and have been named the‘‘fluvial-lacustrine facies association’’ (Bo-hacs et al., 2000).

STRUCTURAL CONTROLS ON BASINEVOLUTION

Recurrent Mesozoic and Cenozoic defor-mation has overprinted nearly all primary latePaleozoic structural features. Nevertheless, attwo localities in the western Turpan-Hami ba-sin, we established independent stratigraphicevidence that defines the timing and sense ofPermian deformation.

Early Permian

The Taoshuyuan fault (Fig. 13) trends northand is herein named informally for a nearbyvillage (TS; Fig 1). This lineament is easilyvisible on high-resolution satellite photo-graphs (Fig. 13), and our detailed geologicmapping demonstrates that the fault juxtapos-es the middle to Upper Carboniferous Liushu-gou Formation on the east at Taodonggou(TD) against Upper Carboniferous through Pa-leogene rocks on the west at Taoxigou (TX).The Taoshuyuan fault dips steeply, and we in-terpret the structure as a high-angle reversefault in its present configuration. The northstrike of this fault contrasts with the trend ofother faults and folds in the area that indicatean overall north-south shortening during theCenozoic (for example, note the overturnedsyncline in the southwest corner of themapped area in Fig. 13).

Lower Permian alluvial-fan deposits of the



Taoxigou Formation at Taoxigou are pre-served immediately west of the fault and in-terpreted as proximal deposits accumulatingadjacent to an ancestral Taoshuyuan fault(Fig. 14). This interpretation is supported byreconnaissance-level observations indicatingthat the number and thickness of conglomeratebeds decreases to the west, along with theirmaximum clast sizes. Sandstone, volcanic,and limestone conglomerate clasts are consis-tent with local derivation from the underlyingCarboniferous Liushugou, Qijiagou, andAoertu Formations (Fig. 14). Rugose coralsand middle Carboniferous fusulinids are pre-served in some limestone clasts (Liao et al.,1987), confirming that the provenance includ-ed marine limestone of the Qijiagou Forma-tion. We interpret the Taoxigou area as thehanging wall of a major Early Permian normalfault, approximately collocated with the Ce-nozoic Taoshuyuan fault (Figs. 13 and 14).Neither the Carboniferous Qijiagou and Aoer-tu Formations nor the Lower Permian Taoxi-gou Formation are present east of the fault atTaodonggou (Fig. 14). Instead, the UpperPermian Daheyen Formation unconformablyoverlies the Upper Carboniferous LiushugouFormation. We interpret that footwall uplift atTaodonggou generated this angular unconfor-mity and that clasts observed to the west, inthe Lower Permian Taoxigou Formation, re-flect erosional unroofing of the Carboniferoussection at Taodonggou.

The Early Permian fault offset was at least2500 m, according to the preserved thickness-es of Carboniferous and Lower Permian strata.An extensional origin for this fault is stronglysupported by the close association in time be-tween the movement along the fault and thelocal extrusion of voluminous volcanic rocks(Fig. 14). In addition, a series of approxi-mately north-trending mafic dikes parallel theTaoshuyuan fault and cut the lower TaoxigouFormation, terminating within the upper mem-ber, suggesting that they fed the Early Permianflows and sills. These dikes are up to 10 mwide, finely crystalline at their centers, andaphanitic at their margins where conglomerateclasts of the Taoxigou Formation are en-trained. Faulting ceased prior to the LatePermian, as evidenced by similar Upper Perm-ian stratigraphy observed at both Taoxigouand Taodonggou (Figs. 13 and 14).

Late Permian

In the western Turpan-Hami basin atAiweiergou (Fig. 1), the Upper Permian Tar-long Formation is deformed in a large foldthat appears contractional in origin. The fold-

ed strata are unconformably overlain by hor-izontally bedded Triassic rocks, thereby defin-ing the deformation as latest Permian or EarlyTriassic (Fig. 15; Greene et al., 2001). Thefold is asymmetric, and structural analysis in-dicates a shallow plunge to the east and over-all south-directed tectonic vergence (Fig. 16).Additional evidence for Upper Permian an-gular unconformities is recorded in limitedseismic data from the western Turpan-Hamibasin, although many lines do not adequatelyresolve the Permian section (Greene et al.,2001).

DISCUSSION

Lithostratigraphic Correlation andPaleogeographic Evolution

Early PermianThe Lower Permian stratigraphic fill of the

Turpan-Hami basin is heterogeneous, contain-ing abundant volcanic rocks and both marineand nonmarine sedimentary rocks. The re-gionally variable lithofacies distribution wascontrolled, at least locally, by structural reliefgiving rise to partitioned subbasins (Figs. 14and 17).

The coarse-grained, proximal TaoxigouFormation in the western Turpan-Hami basinis difficult to correlate regionally. Approxi-mately 200 m of Lower Permian(?) strata alsocrop out in the westernmost Turpan basin(Aiweiergou; Fig. 1) and are tentatively as-signed to the Taoxigou Formation. It is pos-sible that this interval may actually belong tothe Upper Permian Daheyen Formation (Figs.9A and 14). Further understanding of how theTaoxigou Formation correlates to other LowerPermian rocks to the east will require subsur-face data and more detailed structuralmapping.

The Zaobishan and Yierxitu Formationsboth overlie a regional, slightly angular anderosive unconformity (Fig. 14). Although theZaobishan (ZB) and Tian Shan Xiang (TSX)localities are separated by .250 km, the sec-tions are lithostratigraphically similar. Bothunits contain abundant volcanic rocks and in-clude comparable fining-upward trends fromconglomerate and sandstone up through well-laminated mudstone. The increased frequencyof profundal-lacustrine facies suggests a pro-gressively deepening lacustrine basin.

Lower Permian strata in the southern Jung-gar basin are markedly dissimilar to coevalrocks in the Turpan-Hami basin. For example,the Lower Permian stratigraphic record in thesouthern Junggar basin is dominantly marine,including a nearly 1-km-thick interval of

deep-marine turbidites (Fig. 17; Song and Jin,1989; Carroll et al., 1995). These rocks areoverlain by a shoaling sequence several hun-dred meters thick that grades upward fromshallow-marine shelf sedimentary deposits tononmarine fluvial and associated facies (Car-roll et al., 1995). In addition, significant vol-canic rocks are not known from the northernBogda Shan.

Late PermianUpper Permian strata maintain consistent

thicknesses and depositional patterns acrossthe Turpan-Hami basin (Fig. 14). Provenancestudies and diverging paleocurrent data indi-cate that major uplift of the Bogda Shan firstoccurred in the Jurassic (Shao et al., 1999;Greene et al., 2001). Therefore, it has beenproposed that the Turpan-Hami and Junggarbasins were a contiguous sedimentary basinduring Late Permian time (Wartes et al.,2000). This interpretation is supported by gen-erally north-directed paleocurrents in the Up-per Permian Daheyen Formation (Fig. 14) thatindicate that this braided fluvial system pro-graded into the Junggar basin and is equiva-lent to fluvial sandstone and lacustrine rocksof the Wulapo Formation (Figs. 2, 18, and19A). The similarity of lacustrine and associ-ated facies in the two basins also hints at ashared history and a possible throughgoingpaleohydrology.

However, certain aspects of this contiguous-basin hypothesis remain problematic. For ex-ample, the Jingjingzigou Formation in thesouthern Junggar basin is characterized by anevaporative facies association, and biomarkergeochemical attributes indicate hypersalineconditions (Figs. 18 and 19B; Jiang and Fowl-er, 1986; Carroll et al., 1992; Carroll, 1998).The development of underfilled-basin condi-tions contrasts with correlative lake depositsof the Tarlong Formation in the Turpan-Hamibasin, where both sedimentary facies and bio-marker data (Greene, 2000) record a balanced-to overfilled-basin. These lake types could notexist contemporaneously in the same basinand suggest that the Junggar basin was peri-odically partitioned from the Turpan-Hami ba-sin. We hypothesize that hydrologic commu-nication during this phase may have beeninterrupted by structural damming in the vi-cinity of the Bogda Shan (Fig. 19B).

The overlying Lucaogou and Pingdiquan For-mations in the Junggar basin record a balanced-fill lacustrine basin (Carroll and Bohacs,1999). Although thinner, the coeval TarlongFormation in the Turpan-Hami basin recordssimilar conditions, indicating lakes in the twobasins may have coalesced to form the maxi-


WARTES et al.

Figure 10. Detailed measured sections of the lower Upper Permian Tarlong Formation (P2t) along the northern Turpan-Hami basin.Sections are presented from west to east (see Fig. 1 for locations and Fig. 3 for legend).



Figure 10. (Continued.)


WARTES et al.

Figure 11. Outcrop photographs of the Up-per Permian Tarlong Formation. (A) Ex-ample of outcrop extent and quality in theTarlong Formation in the western Turpan-Hami basin at Aiweiergou (note person atleft-center for scale). (B) Complete crosssection of a fluvial channel in the TarlongFormation at Aiweiergou.

Figure 12. Measured sections of the uppermost Permian Quanzijie (P2q), Wutonggou(P2wt), and Guodikeng (P2g) Formations of the Lower Cangfanggou Group (P2c), north-ern Turpan-Hami basin. Sections are presented from west to east (see Fig. 1 for locationsand Fig. 3 for legend).

mum paleogeographic expanse of Late Perm-ian lakes (Fig. 18). The underlying cause ofthis change is not clear, but may be related tolake-level rise and the reintegration of drain-ages previously confined to the Turpan-Hamibasin (Fig. 19C). The uppermost PermianCangfanggou Group records the developmentof overfilled lacustrine and fluvial settings. Inaddition, the marked change in stratal thick-ness between the two basins is no longer ev-ident during this phase (Fig. 19D). We pro-pose that this trend toward an overfilled basinwas largely controlled by decreasing subsi-dence and potential accommodation (cf. Car-roll and Bohacs, 1999).

CONSTRAINTS ON THE TECTONICEVOLUTION OF NORTHWEST CHINA

Early Permian Extension

Permian extension of regions north of theTian Shan has been proposed in several pre-vious studies (e.g., Hsu, 1988; Peng andZhang, 1989; Allen et al., 1991). Unfortunate-ly, data capable of testing these hypotheseshave generally been sparse. Seismic data from



Figure 13. Geologic map of the Taoshuyuan area (see Fig. 1 for location). Field mapping was conducted by using a Corona (KH-4B)satellite photograph (Entity Identification DS1109–2233dF059) and handheld GPS receivers. Minimum spatial resolution of the satellitephotograph is ;3 m. The map was corrected to Mercator projection by reference to landmarks depicted on a 1:200 000 topographicmap. Note the location of the Taoshuyuan fault, interpreted by us to be a major down-to-the west, Early Permian normal fault.Stratigraphic relationships between the west side of the fault (Taoxigou; TX) and east side (Taodonggou; TD) are shown in Figure 14.


WARTES et al.

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Figure 15. Outcrop photograph of the angular unconformity separating lower UpperPermian rocks of the Tarlong Formation (P2t) from Triassic strata at Aiweiergou in thewestern Turpan-Hami basin (see Fig. 1 for location). Stratigraphic relationships indicatethat the folding occurred in latest Permian to Triassic time. Note large truck in lowercenter for scale.

Figure 16. Structural data (corrected forpost-Triassic deformation) from the fold atAiweiergou (Fig. 15), indicating an eaststrike for the structure and vergence to thesouth.

the northern Junggar basin image a northwest-trending half-graben structure, which repre-sents the most commonly cited evidence forextensional tectonism (Bally et al., 1986; Liu,1986; Peng and Zhang, 1989). However, nocorrelations or local well data have been pub-lished that demonstrate a Permian age for thegraben fill. Small normal faults have been re-

ported from the northwestern and southwest-ern Turpan-Hami basin, although the ages ofthe structures are undetermined (Allen et al.,1993b). Poorly dated diffuse magmatism northof the Tian Shan has also been cited as evi-dence for Permian–Triassic extension in north-western China (e.g., Allen et al., 1991). Thegeochemistry of tholeiitic basalts intrudingLower Permian sedimentary deposits indicatesan enrichment in incompatible trace elements,a trend consistent with magmatism in an ex-tensional setting (Allen et al., 1991).

An alternative model involves Late Permianto Early Triassic(?) extension related to in-ferred regional sinistral shear zones (Allen etal., 1995). This intriguing hypothesis is basedon tectonic reconstructions that imply large-scale relative movement of the East Europeanand Angara cratons (Sengor et al., 1993; Sen-gor and Natal’in, 1996). In this scenario, theboundary forces set up by the interaction ofthese two domains produced counterclockwiserotation and differential subsidence of coupledcrustal blocks, including the Turpan-Hami ba-sin (Allen et al., 1995). This transtensional hy-pothesis is partly supported by some existingpaleomagnetic measurements (Li et al., 1991)and relies to a large degree on projections ofstructural relationships defined within the for-mer Soviet Union.

Geohistory analyses indicate that subsi-

dence of the southern Junggar basin reacheda maximum during the Late Permian (Carrollet al., 1990, 1995)—temporally consistentwith the Allen et al. (1995) model. However,the stratigraphic data collected in this studyfrom the Turpan-Hami basin do not agree withthe Late Permian–Early Triassic timing pro-posed by Allen et al. (1995). We identified aclose association of hypabyssal volcanic rocksstrictly with Lower Permian strata (Fig. 14).There remains a dearth of radioisotopic agecontrol on these rocks, although Wartes (1999)reported an 40Ar/39Ar age of 272 6 1.16 Mafrom plagioclase phenocrysts in andesite sam-pled in a subsurface well in the western Turpan-Hami basin. In addition, our mapping dem-onstrates that extension along the Taoshuyuanfault was confined to the Early Permian (Figs.14 and 17).

The final consolidation of the Tian Shan,south of the Turpan-Hami basin, occurred inthe Late Carboniferous–earliest Permian (e.g.,Allen et al., 1993a; Carroll et al., 1995; Zhouet al., 2001). However, postcollisional, north-south convergence likely continued well intothe Permian (e.g., Carroll et al., 1990, 1995).Synsedimentary deformation of uppermostCarboniferous to lowest Permian(?) turbiditeshas been observed in the northwestern Tur-pan-Hami basin, where isoclinal folds occurbetween unfolded horizons (Allen et al.,1991). In addition, because no post–EarlyPermian magmatism has been documented inthe region, the age of other folds and faults inthese turbidites is limited to the late Paleozoicby postdeformational intrusion of dikes (Allenet al., 1993).

Similar relationships, which otherwise ap-pear antithetical, are known from a variety ofPhanerozoic orogens (e.g., Durand et al.,1999, and references therein). However, manycommonly attributed explanations for exten-sion in convergent settings are difficult to ap-ply to the Turpan-Hami region. For example,processes such as subduction-zone retreat(Royden, 1993) and related mantle upwelling(Cavinato and DeCelles, 1999) require contin-ued subduction during retrograde motion ofthe slab to generate upper-plate extension.Subduction-related arc volcanism, representedby the Liushugou Formation in the BogdaShan, clearly ceased in the Carboniferous.This arc massif was subsequently eroded andunconformably overlain by Lower Permianrocks at Zaobishan and Tian Shan Xiang(Figs. 14 and 17).

Another problematic aspect presented bythe Taoshuyuan structure is its north-south ori-entation, a trend orthogonal to the sutures tothe south. Arc-parallel extension is known


WARTES et al.

Figure 17. Schematic Early Permian paleogeography and tectonic setting of the greaterTurpan-Hami-Junggar region. Refer to Figure 2 for Lower Permian formation abbrevi-ations and to Figure 14 for explanation of Carboniferous units.

from obliquely convergent margins (e.g., theAleutians, Ave Lallemant and Oldow, 2000).However, again, the timing of extension in theTurpan-Hami basin significantly postdated ac-tive subduction. Extensional structures, suchas the Upper Rhine and Lake Baikal rifts, dotrend at a high angle to collisional zones andmay be genetically related, reflecting tensilestress normal to applied compression (e.g.,Molnar and Tapponnier, 1975; Sengor et al.,1978; Hancock and Bevan, 1987).

An alternative explanation is that extension atTaoshuyuan is a pull-apart structure related tostrain-partitioning driven by strike-slip motion.Although the kinematic considerations in the Al-len et al. (1995) model did not predict the dom-inant phase of Early Permian extension, neitherdid they discount the potential for an earliercompound history. In addition, Chen et al.(1999) argued that the Tian Shan was an obliquecollisional orogen in which regional strike-sliptectonics might be expected. The greater Jung-gar-Turpan-Hami region is bound to the southby the North Tian Shan fault that displays abun-dant indicators of dextral shear (Fig. 17). 40Ar/39Ar analysis of neomorphic muscovite frommylonite within the shear zone produced an ageof 269 6 5 Ma, demonstrating active strike-slipmotion during the Early Permian (Shu et al.,1999). Intervening crust may have been escap-

ing eastward toward regions where the Paleo-tethys was still undergoing active subduction.Similar tectonic models involving escape andconcomitant extension have been proposed byRoyden (1993) and Mann (1997).

Further, more detailed work is clearly re-quired to fully evaluate the tectonic controlson Early Permian extension of the Turpan-Hami basin. Decades of research in other re-gions displaying a bimodal stress regime, suchas the greater Mediterranean-Carpathian sys-tem, have illustrated the comprehensive levelof structural data required to address aspectsof large-scale geodynamic evolution (e.g.,Wortel and Spakman, 2000).

Late Permian Flexural Foreland-BasinDevelopment

Many previous studies have interpretedPermian basin subsidence in northwesternChina as a flexural response to thrust loadingin Tian Shan (Watson et al., 1987; Graham etal., 1990; Carroll et al., 1990, 1995; Allen etal., 1993a). Neither Late Permian volcanismnor Late Permian extensional faulting hasbeen documented, allowing for the possibilitythat Upper Permian strata accumulated in aforeland basin. This interpretation requiresthat the regional tectonic setting that generated

the Early Permian extension at Taoshuyuanand the magmatism throughout the Turpan-Hami basin changed to support a more north-vergent fold-and-thrust belt in the north TianShan.

A change in tectonic regime is recorded bythe cessation of Early Permian dextral motionon the North Tian Shan fault. Instead, theshear zone was overprinted by subsequent,brittle, north-vergent thrusting (Shu et al.,1999). This transition also coincided with alarge-scale reversal in strike-slip kinematicsinferred across central Asia (Allen et al.,1995). The major unconformity at the base ofthe Upper Permian and the northward progra-dation of the coarse-clastic Daheyen Forma-tion are consistent with increased uplift of theancestral Tian Shan. This northward prograd-ing wedge is recorded by paleocurrents (Fig.14) and by proximal debris-flow deposits inthe south (Aiweiergou; Fig. 1) that gradenorthward into braided fluvial deposits (Fig.19A). Tectonic subsidence of the southernJunggar basin also accelerated during the LatePermian, creating accommodation for .4000m of nonmarine sediments (Fig. 18; Carroll etal., 1995).

In our opinion, the available evidence bestsupports the foreland-basin model proposed byGreene et al. (2001) that interprets the UpperPermian strata of the Turpan-Hami region aswedge-top deposits with respect to the northTian Shan fold-and-thrust belt. This model isconsistent with the loci of maximum accom-modation—i.e., the foredeep—occurring be-yond the active structural front in the southernJunggar basin (Fig. 19). The mineral immatu-rity of Upper Permian sandstone (Carroll et al.,1995; Shao et al., 2001; Greene, 2000), variablepaleocurrents (Fig. 14), and increased erosionaltruncation and tapering toward the hinterland(Fig. 18) are all common features of wedge-topdeposits (DeCelles and Giles, 1996). In addi-tion, because wedge-top deposits are kinemat-ically associated with the growth of the oro-genic wedge, strata are commonly deformedshortly after deposition—akin to the fold atAiweiergou in the western Turpan-Hami basin(Fig. 15). Lake deposits, similar to those ob-served in the Turpan-Hami basin, can also formin wedge-top basins when drainages becomeimpounded (e.g., Horton, 1998). In fact, the ep-isode of basin underfilling recorded by the Ji-ngjingzigou Formation in the southern Junggarbasin may reflect structural damming during lo-cal uplift of the orogenic wedge or propagationof a new frontal thrust (Fig. 19B; e.g., Lawtonand Trexler, 1991).

Preservation and identification of thiswedge-top zone is often complicated in the



Figure 18. Regional south-north lithostratigraphic cross section correlating Upper Permian rocks between the Turpan-Hami and Junggarbasins (see Fig. 1 for locations). Correlation is based on lithofacies considerations and previously constructed basinwide stratigraphiccharts (e.g., Peng and Zhang, 1989; Chen et al., 1985). Section datum is the base of the Lower Cangfanggou Group. Data for Aiweiergou(AR) are from this study; data for North Tian Shan (NT) are from Hu Ting (1998, written commun.); South Junggar (SJ) is a compositesection based on exposures at Tianchi and Urumqi (TI and UR; Fig. 1; Liao et al., 1987; Carroll et al., 1995); Huoshaoshan (HU) andXidagou (XD) sections through the Jiangjunmiao Formation (P2jg) and the Pingdiquan Formation (P2p) were studied in the northeasternJunggar basin at Huoshaoshan (HU) and Xidagou (XD) by XPGEG (1991) and Tang et al. (1997). See Figure 2 for Upper Permianformation abbreviations in the Turpan-Hami and southern Junggar basins.

geologic record by continued uplift of the oro-genic wedge and cannibalization of wedge-topsediments (DeCelles and Giles, 1996). Thesomewhat unusual preservation of the LatePermian Turpan-Hami basin likely reflects thelow degree of erosional unroofing during theMesozoic and Cenozoic. Instead, several sub-sequent phases of intracontinental foreland-ba-sin development were superimposed over theTurpan-Hami and Junggar basins (e.g., Hendrixet al., 1992; Graham et al., 1993). Therefore,the unique polycyclic tectonic history of north-west China may have inhibited erosional re-cycling of the Permian sedimentary record.

CONCLUSIONS

The sedimentary fill of the Turpan-Hamibasin records a distinct change in basin con-figuration between the Early and Late Perm-ian. Lower Permian stratigraphy is heteroge-neous and includes abundant volcanic flows

and sills. In addition, basin evolution is con-trolled at one locality by .2500 m of motionalong a basin-bounding normal fault. The sed-imentary, structural, and magmatic evidenceindicates an episode of active extensional tec-tonics. Some of these features trend normal tothe east-trending Late Devonian–Carbonifer-ous collisional sutures that generated the an-cestral Tian Shan and may have been drivenby continued north-south compression that ac-commodated west-east extension.

Upper Permian strata are separated fromLower Permian sections all along the northernTurpan-Hami basin by a regional unconfor-mity, marking the beginning of the secondphase in basin evolution. In contrast to theLower Permian rocks, Upper Permian strata areamagmatic, exclusively nonmarine, and rela-tively uniform in thickness across the Turpan-Hami basin. Extensive braided fluvial depositscharacterize the lower Upper Permian and areoverlain by fluctuating lacustrine-fluvial de-

posits. The paleogeography of this later phaseincluded the coalescence of a regional lacus-trine depositional system that included thelarger Junggar basin. The rapid northwarddeepening of this composite basin is best ex-plained as flexural subsidence in a foreland-basin setting, placing the Turpan-Hami basinin a wedge-top position, adjacent to the northTian Shan. Uplift of the orogenic wedge ex-erted significant control on the evolution oflake types in the region, periodically partition-ing the Turpan-Hami and Junggar basins.

ACKNOWLEDGMENTS

This study reports on field expeditions to the Tur-pan-Hami basin conducted during the summers of1996–1998, in collaboration with the TUHA [Tur-pan-Hami] Research Institute for Petroleum Explo-ration and Development and its parent, the ChineseNational Petroleum Company. Director ZengXiaoming and Chief Geologist Wang Wuhe deservespecial mention for their help. Cheng Keming, HuTing, Marc Hendrix, Angela Hessler, and Yongjun


WARTES et al.

Figure 19. Schematic time series (T1 through T4) illustrating the Late Permian paleogeographic evolution of the Junggar and Turpan-Hami basins and interpreted tectonic controls of basin evolution. Locations of Aiweiergou (AR), Tianchi (TI), and Zaobishan (ZB) arein Figure 1; NTS refers to the geographic northern Tian Shan. See Figure 2 for formation abbreviations. Northern Junggar basin unitsinclude the Jiangjunmiao Formation (P2jg) and the Pingdiquan Formation (P2p). (A) Progradation of Daheyen Formation clastic wedge.(B) Interpreted partitioning of the Turpan-Hami basin lake (lower Tarlong Formation) from the Junggar basin lake (JingjingzigouFormation). (C) Maximum expansion of the lacustrine conditions in the Turpan-Hami and Junggar basins. (D) Overfilled-basin condi-tions marked by increasing fluvial influence.

Yue are thanked for their valuable aid in the field.We are grateful for the insightful advice and assis-tance of E. Zhang and S. Graham. This paper alsobenefited from discussions with B. Tikoff, M.Rhodes, J. Pietras, and C. Waters. Thoughtful re-views by P. DeCelles and B. Ritts greatly improvedthe manuscript. This research was supported bygrant 33005-AC8 from the Donors of The Petro-leum Research Fund (PRF), administered by theAmerican Chemical Society. Support for T. Greenewas provided by PRF grant 32605-AC2 and theStanford-China Industrial Affiliates, including Agip,ARCO, Chevron, Exxon-Mobil, JNOC, Phillips,Shell, Statoil, Texaco, and Triton. Additional sup-port at the University of Wisconsin—Madison forresearch on lacustrine sedimentary basins was pro-vided by Conoco and Texaco. We also acknowledgefunding from the Graduate School of the Universityof Wisconsin—Madison.

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