Permian Lacustrine Deposits of Northwest China, in E

Home , Dicynodon, Geology of China, Hami, Junggar Basin, Northwest China

Wartes, M. A., A. R. Carroll, T. J. Greene, Kerning Cheng, and Hu Ting, 2000, Permian lacustrine deposits of northwest China, in E. H. Gierlowski- Kordesch and K. R. Kelts, Eds., Lake basins through space and time: AAPG Studies in Geology 46, Chapter 8 p.123-132. Permian Lacustrine Deposits Of Northwest China

Marwan A. Wartes Alan R. Carroll Department of Geology and Geophysics, University of Wisconsin-Madison Madison, Wisconsin, U.S.A.

Todd J. Greene Department of Geological and Environmental Sciences, Stanford University Stanford, California, U.S.A.

Kerning Cheng Research Institute of Petroleum Exploration and Development, China National Petroleum Corporation Beijing, People's Republic of China

Hu Ting Research Institute of the Tu-Ha Petroleum Exploration and Development Bureau, China National Petroleum Corporation Hami, People's Republic of China

INTRODUCTION Turpan-Hami basins (Figures 1, 2) (Hendrix et al., 1992; Greene et al., 1997, in press; Shao et al., 1999); therefore, Permian deposits of the Junggar and Turpan-Hami the Bogda Shan provide an oblique cross-section of Per- basins of the Xinjiang Uygur Autonomous Region of mian lake deposits of the unified Junggar-Turpan-Hami northwest China preserve some of the thickest and most basin. In addition to lacustrine sedimentation, the south- areally extensive lake strata on Earth. In the south Jung- ern margins of this basin periodically received coarse clas- gar depocenter, these nonmarine deposits are up to 5 km tic sediments shed from the ancestral Tian Shan (Figure 1) thick and organic-rich facies rank among the thickest (Carroll et al., 1990, 1995; Greene et al., 1997). Coarse clas- and richest petroleum source rocks in the world (Gra- tics were also shed southward into the basin from the ham et al., 1990; Lawrence, 1990; Demaison and Kelameili and west Junggar Shan, uplifts bounding the Huizinga, 1991; Carroll et al., 1992). In addition, Permian northeastern and northwestern edges of the basin respec- lacustrine deposits are estimated to span 1000 km along tively (Figure 1) (Lee, 1985; Carroll et al., 1990; Tang et al., strike, indicating that widespread lakes represented a 1997a; and Zhao and Tang, this volume). major paleogeographic feature of central Asia (Figure 1). Up to 5 km of total Permian subsidence is recorded Unfortunately, the remote location of these deposits has over a 40-50 m.y. span, yet the tectonic significance of this hindered detailed studies, and the western literature basin remains controversial. Hypotheses provided to contains only sparse reference to this important record explain Permian subsidence are numerous, often mutually of continental sedimentation. The purpose of this paper incompatible, and reflect the paucity of first-hand geo- is to briefly review the Permian nonmarine stratigraphy logic observations available to constrain the Permian and report on recent field-based studies documenting tectonic setting. Proposed hypotheses range from fore- the Permian lacustrine stratigraphy exposed along the land basin flexure (Watson et al., 1987; Carroll et al., north and south flanks of the Bogda Shan (Figure 2). 1995), to extension (Bally et al., 1986; Allen et al., 1991), to regional transtension (Allen et al., 1995). SETTING STRATIGRAPHY Paleocurrents and other data indicate that the development of Permian lakes pre-date the uplift of the The Junggar and Turpan-Hami basins portray a Bogda Shan, which now partitions the Junggar and complicated association of facies, particularly between 123 Figure 1—Simplified geologic map of the Junggar and Turpan-Hami basins illustrating the distribution of Permian outcrops (modified from Chen et al., 1985) and the known extent of Permian lacustrine facies. Box indicates the location of Figure 2. Permian Lacustrine Deposits of Northwest China 125

Figure 2—Location map of study area depicting Permian outcrops (modified from Chen et al., 1985). Strati- graphic details for named localities are shown in the regional correlation (Figure 3). Note paleocurrent data taken from clast imbrications and trough cross-beds indicating a north-northeasterly paleoflow (Carroll, 1991; Carroll et al., 1995; Greene et al., in press). These data are inconsistent with a Permian physiographic expres- sion of the Bogda Shan, supporting a hypothesis for a united Permian lake basin spanning both the Junggar and Turpan-Hami basins. lake marginal and basinal environments. In addition, Group are exposed at Zaobishan (Greene et al., 1997; precise understanding of the temporal framework for Wartes et al., 1999) (Figures 2, 3). The section consists these deposits is limited and regional correlations, of fine-grained sandstones, limestones, and dark such as that shown in Figures 3 and 4, await further gray calcareous mudstones organized in a series of detailed work. Nonetheless, a synthesis of existing and parasequences 1-3 m thick. These cycles generally new data are summarized in a basin-oblique west to grade upward from stromatolitic limestone, to lami- east chronostratigraphic cross-section of the Permian nated mudstones, and are capped by a coarsening- (Figure 3). The stratigraphy and physical characteris- upward succession of siltstone to fine-grained tics illustrated by the correlation allow for a simplified sandstone. This cyclicity is interpreted to reflect tripartite division of these deposits into phases of transgressive-regressive fluctuations in lake-level lacustrine development (Figure 3). (Wartes et al., 1998), perhaps in response to varying climatic aridity. Several 20-30 m intervals of Lower LOWER PERMIAN Permian lacustrine facies have also been documented in the eastern end of the Turpan-Hami basin The first phase of lacustrine deposition spans the at Tian Shan Xiang (Figures 2, 3, 5). They are Lower Permian and is the least well documented, having expressed as laminated, dark gray mudstone con- been noted in just two localities along the Bogda Shan taining fish scales, algal lamination, and localized (phase I on Figure 3). These deposits follow an overall soft-sediment deformation (Figure 5). marine regression marked by a diachronous retreat of The Early Permian age designation for these marine waters from the region. Marine deposition deposits is based largely on stratigraphic position; continued in deeper portions of the basin, particularly however, interbedded volcanic rocks occur at both near the south Junggar depocenter, well into the Early localities (Figure 3). Future radiogenic age determina- Permian (Carroll et al., 1990) (Figure 3). tions of these igneous rocks will provide a critical con- An 80 m thick succession of lacustrine rocks of the trol on the chronostratigraphy of Lower Permian Lower Permian Yierxitu Formation of the Aqibulake lacustrine deposits. Figure 3—Permian chronostratigraphic correlation along a basin-oblique transect of the Bogda Shan. Localities are from the southern Junggar (northern Bogda Shan), western Turpan-Hami (northern Tian Shan), and northern Turpan-Hami (southern Bogda Shan) areas. Lacustrine development can be divided into three phases, which are shown at right as I, II, and III, and correspond to the organization of the text description. The phases are based on age relationships, sedimentary facies, lake type, and other diagnostic characteristics. Note the indicated stratigraphic location of detailed sections displayed in Figure 5. Distances between localities are not shown; refer to Figure 2 for true lateral separation. Formation subdivisions and regional nomenclature are shown in Figure 4. Permian Lacustrine Deposits of Northwest China 127

Figure 4—Subdivision and correlation of Permian units in the Junggar and Turpan-Hami basins (modified from Zhao, 1982; Chen et al., 1985; and Liao et al., 1987).

LOWER-UPPER PERMIAN 1992; Clayton et al., 1997; Carroll, 1998). Another potential source for these oils is the slightly older Pingdiquan The next phase of lacustrine development (labeled II Formation of the northeastern Junggar basin (Tang et al., on Figure 3) is early-Late Permian in age and has 1997a) (Figure 4). The Jingjingzigou Formation is slightly received the most attention due to the extremely rich more fossiliferous than the Wulapo Formation with source rocks occurring in this interval along the north- reports of numerous ostracode genera including Tomiella, west flank of the Bogda Shan (Graham et al., 1990; Car- Darwinula, and Darwinuloides, as well as palynomorphs roll et al., 1992, 1998). Recent studies have begun to such as Cordaites sp. (Zhang, 1981; XPGEG, 1991). correlate these organic-rich facies with widespread, The Jingjingzigou Formation grades upward into coeval lacustrine mudstones preserved south of the the thick oil shales characteristic of the Lucaogou For- Bogda Shan in the Turpan-Hami basin (Greene et al., mation (Figure 5). The Lucaogou Formation consists of 1997; Wartes et al., 1998). The following description of more than 800 m of finely laminated, organic-rich this phase of lacustrine deposition will begin with rocks mudstone. Dolomite also occurs as occasional nodular of the Upper Jijicao Group in the southern Junggar beds and as cement in very fine to fine-grained sand- basin, followed by equivalent strata of the Taodonggou stones. Total organic carbon (TOC) commonly exceeds Group in the Turpan-Hami basin. This separation is 20% in the richest facies and averages 4% over one 800 m warranted due to the differing formation names and, to interval (Carroll et al., 1992). Coeval organic-rich a lesser degree, lithologic character (Figures 3, 4). lacustrine facies of the Pingdiquan Formation (Figure 4) are the dominant source rocks in the subsurface of the northeastern Junggar basin (Peng and Zhang, 1989; Upper Jijicao Group Tang et al., 1997a), implying a widespread distribution The lower Upper Permian section of the southern of lacustrine strata correlative to the Lucaogou Forma- Junggar begins in the Wulapo Formation with variable tion. The organic richness, biomarker characteristics, amounts of sandstone, rippled siltstone, and plane- and lack of bioturbation all suggest deposition in a laminated mudstone interpreted to represent shallow deep, stratified lake with anoxic bottom waters. oxic lacustrine deposition interbedded with occasional Deposits of the Lucaogou Formation differ from many fluvial deposits (Carroll et al., 1995). Fossils reported other organic-rich lacustrine facies, however, in that from the Wulapo are rare but include the bivalve they were deposited at a relatively high paleolatitude Palaeonodonta pseudolongissima and flora such as (39-43°N) (Sharps et al., 1992; Nie et al., 1993) and in Walchia sp., Dadoxylon teilhardii, and Paracalamites sp. low to moderately productive lakes (Carroll, 1998). (Liao et al., 1987; XPGEG, 1991). The Lucaogou Formation is rich in fossils including The Wulapo Formation grades up into siltstones, fish, such as Cichia sp., Tienchaniscus longipterus, and mudstones, and fine-grained sandstones of the Turfania taoshuyuanensis; bivalves Anthraconauta Jingjingzigou Formation. The Jingjingzigou Formation is pseudophilipsii and A. iljinskiensis; ostracods Darwinula characterized by highly visible outcrop cyclicity punctu- parallela, D. monitoria, Darwinulides ornata, and ated by periodic desiccation surfaces (Figure 5). Bio- Sinusuella polita; and flora including Rufloria (Neog- marker geochemistry of mudstone extracts record a gerathiopsis) derzavinii and Paracalamites sp., (Zhang, specialized, salinity-tolerant biota, which, when consid- 1981; Liao et al., 1987; Carroll et al., 1992). ered in concert with other physical characteristics such as Overlying the Lucaogou is the Hongyanchi Forma- mudcracks and diagenetic dolomite, may suggest evapo- tion, which includes nonlaminated mudstone, lime- rative conditions (Carroll et al., 1992; Carroll, 1998). stones, and conglomerates, Pebble imbrications from Hypersaline facies similar to the Jingjingzigou Formation within the conglomerates exposed near Urumqi are the appear to have generated the oils produced from the source of one of the paleocurrent insets in Figure 2. The giant Karamay and related fields along the northwestern Hongyanchi Formation is generally Interpreted as being margin of the basin (Jiang and Fowler, 1986; Carroll et al,, deposited in freshwater lakes that were associated with 128 Wartes et al.

Figure 5—Representative sections of Permian lacustrine deposits in northwest China (see Figure 2 for locations and Figure 3 for stratigraphic position). All measured section thicknesses are expressed in meters. (A) Detailed measured section of the Lower Permian exposures of the Yierxitu Formation exposed in the easternmost Turpan-Hami basin at Tian Shan Xiang. (B) Schematic stratigraphy of the lower-Upper Permian upper Jijicao Group of the southern Junggar basin (modified from Liao et al., 1987; Carroll et al., 1992, 1995). (C) Detailed measured section of the upper portion of the lower Upper Permian Tarlong Formation of the Turpan-Hami basin exposed at Zaobishan along the south-central Bogda Shan. (D) Detailed measured section of the lower portion of the Upper Permian Quanzijie Formation of the lower Cangfanggou Group exposed in the southeastern Bogda Shan at Tian Shan Xiang. Permian Lacustrine Deposits of Northwest China 129 fluvial systems (Carroll et al., 1992; Carroll, 1998). The Guodikeng formations of the lower Cangfanggou Hongyanchi Formation is also fossiliferous containing Group (phase III on Figure 3). As noted by Tang et al. the palynomorphs Cordaitina and Hamiapollenites; (1994), the lower Cangfanggou Group is a highly vari- bivalves Anthraconauta ilijinskiensis and Microdontella able lithostratigraphic unit. Conglomerate intervals elliptica; ostracodes such as Darwinuleides ornata; and range from organized to weakly organized deposits the plant Pecopteris anthriscifolia (Yang et al., 1986; and are often associated with pebbly sandstones. Well- XPGEG, 1991). bedded sandstones, rippled siltstones, and thinly bedded carbonates are common (Figure 5). A variety of Taodonggou Group fine-grained intervals are also present throughout the lower Cangfanggou Group. The heterogeneous The Daheyen Formation, preserved farther south in lithologies reflect a variety of depositional environ- the Turpan-Hami basin, is recorded by thick sections of ments and flow regimes, including alluvial, braided conglomerates and minor sandstones (Figure 3). Fine- and meandering fluvial, and shallow lacustrine (Yang grained facies are very rare but have been reported from et al., 1986; Zhao et al., 1991; Tang et al., 1994, 1997b). one well in the southern Turpan (Greene et al., 1997) and This phase of lake development was dominated by in the easternmost locality at Tian Shan Xiang (Figure 3). freshwater lacustrine systems, effectively continuing We interpret the Daheyen Formation to be approxi- the trend of decreasing salinity noted in the previous mately time-equivalent to the Wulapo and Jingjingzigou interval. Correlation of these strata from both sides of formations deposited farther north, although biostrati- the Bogda Shan is facilitated by the best developed graphic verification of this correlation is still pending biostratigraphy of all three phases. In particular, many (Figure 3). The Daheyen Formation is often well orga- Chinese researchers have focused on characterizing nized with pebble imbrications and trough cross-stratifi- conformable Permian-Triassic boundary sections that cation, both of which form the basis for paleocurrent are well-exposed along the northern flank of the measurements along the southern margin of the Bogda Bogda Shan (e.g., Liu, 1993; Cheng, 1993), compiling Shan (Figure 2). Sedimentologic features and strati- impressive fossil lists consisting of dozens of flora and graphic style suggest deposition within braided fluvial fauna. Typical fossils include a diverse assemblage of systems derived from exposed Carboniferous rocks of flora, such as Callipteris zeilleri, Comia dentata, Iniopteris the ancestral Tian Shan. sibirica, and Pecopteris anthriscifolia; bivalves Palaeon- The Daheyen Formation grades up into the Tarlong odonta psuedolongissima, P. parallela, P. fischeri, and Formation, which is well exposed in several localities Microdontella plotnikovskiensis; ostracodes such as Dar- along the southern flanks of the Bogda Shan (Figures 2, winula implana, D. kuznetskiensis, and Darwinuloides 3). The Tarlong is characterized by numerous coarsening dobrinkaensis; and several Late Permian vertebrates upward cycles that begin with mudstones and siltstones including Dicynodon tienshanensis, Jimusaria sinkiangen- and grade up through coarse sandstone or conglomerate sis, and Kunpania scopulusa (see Yang et al., 1986, for (Figures 3, 5). This unit also contains several limestone complete listing). intervals, many of which are fossiliferous, preserving bivalves, gastropods, and fish such as Turfania taoshuyuanensis. The Tarlong is interpreted as varying from pro- DISCUSSION fundal lacustrine facies to cyclic lake-marginal facies, Rapid Permian subsidence allowed for the preser- which periodically shallow up into fluvial deposits (Fig- vation of areally extensive lacustrine deposits cover- ure 5) (Wartes et al., 1998). Several coarsening-upward ing approximately 200,000 km2 of central Asia. These packages are suggestive of prograding deltaic sedimen- lake deposits reach thicknesses approaching 2000 m tation. Biostratigraphic control in Tarlong Formation is and thus represent one of the most impressive, yet also poor; however, the upper age is limited by overlying least well understood, accumulations of lacustrine rocks of the Lower Cangfanggou Group, which contain strata on Earth. The association of Lower Permian well-described, age diagnostic fauna and flora (Yang et lacustrine facies with volcanic rocks (see Figure 3) is al., 1986; Liao et al., 1987). most consistent with rift-related basin subsidence dur- Regional lower Upper Permian lake deposits, particu- ing this time; however, the thickest nonmarine larly those exposed on the northwest flank of the Bogda deposits, presumably responding to the maximum Shan, portray an overall decrease in salinity through rate of subsidence, were deposited during the Late time. This trend is indicated by early, more hypersaline Permian. Preliminary thermal history modeling based deposits of the Jingjingzigou Formation which grade up on stratigraphic thicknesses and vitrinite reflectances into the deeper basinal laminated facies of the Lucaogou in the northwest Bogda Shan does not support the Formation, and finally up into more freshwater condi- existence of elevated Permian heat flows anticipated tions recorded by the preservation of several intervals of in a rift environment (Carroll et al., 1992; see also King fossiliferous freshwater limestones in the Hongyanchi et al., 1994). Finally, folds exposed beneath a sub-Mid- and upper Tarlong Formations (Figure 3). dle Triassic angular unconformity in the western Tur- pan basin appear to have been compressional in UPPER-UPPER PERMIAN origin (Wartes et al., 1998). These apparent contradic- tions suggest a complex basin history, possibly The final phase of lacustrine deposition occurs in related to regional strike-slip tectonics as suggested the uppermost Permian Quanzijie, Wutonggou, and by Allen et al. (1995). 130 Wartes et al.

ACKNOWLEDGMENTS Xinjiang Uygur Autonomous Region, Scale 1:2,000,000: Beijing, Geologic Publishing House. This research was supported by a grant from the Cheng, Z., 1993, On the discovery and significance of Donors of The Petroleum Research Fund, adminis- the nonmarine Permo-Triassic transition zone at tered by the American Chemical Society. Additional Dalongkou in Jimusar, Xinjiang, China, in S. G. support was provided by the Stanford-China Indus- Lucas and M. Morales, eds., The Nonmarine Trias- trial Affiliates, including Agip, Arco, Chevron, Exxon, sic: New Mexico Museum of Natural History & Sci- JNOC, Mobil, Phillips, Shell, Statoil, Texaco, and Tri- ence Bulletin No. 3, p. 65-67. ton. We also acknowledge funding from the Graduate Demaison, G., and B. J. Huizinga, 1991, Genetic classifi- School at the University of Wisconsin-Madison. We cation of petroleum systems: AAPG Bulletin, v. 75, are grateful for the insightful advice and assistance of p. 1626-1643. S. A. Graham. We thank A. Hessler and Yongjun Yue Graham, S. A., S. Brassell, A. R. Carroll, X. Xiao, for their valuable field assistance. This paper benefited G. Demaison, C. L. McKnight, Y. Liang, J. Chu, and M. from reviews by K. Kelts and J. Parnell. S. Hendrix, 1990, Characteristics of selected petroleum source rocks, Xinjiang Uygur Autonomous Region, northwest China: AAPG Bulletin, v. 74, p. 493-512. REFERENCES CITED Greene, T. J., A. R. Carroll, and M. S. Hendrix, 1997, Permian-Triassic basin evolution and petroleum Allen, M. B., B. F. Windley, C. Zhang, Z. Y. Zhao, and system of the Turpan-Hami basin, Xinjiang G. R. Wang, 1991, Basin evolution within and adja- Province, Northwest China: AAPG Annual Meeting cent to the Tien Shan range, NW China: Journal of with Abstracts, v. 6, p. 42. the Geological Society, London, v. 148, p. 369-378. Greene, T. J., M. S. Hendrix, A. R. Carroll, and S. A. Allen, M. B., A. M. C. Sengor, and B. A. Natal'in, 1995, Graham, in press, Middle to Late Triassic uplift of Junggar, Turfan and Alakol basins as Late Permian the Bogda Shan: constraints on initial partitioning to ?Early Triassic extensional structures in a sinis- of the Turpan-Hami and southern Junggar Basins, tral shear zone in the Altaid orogenic collage, cen- Xinjiang Uygur Autonomous Region, NW China, in tral Asia: Journal of the Geological Society, London, M. S. Hendrix and G. A. Davis, eds., Paleozoic and v. 152, p. 327-338. Mesozoic tectonic evolution of central Asia—from Bally, A. W., I. M. Chou, R. Clayton, H. P. Eugster, continental assembly to intracontinental deforma- S. Kidwell, L. D. Meckel, R. T. Ryder, A. B. Watts, tion: GSA Special Paper. and A. A. Wilson, 1986, Notes on sedimentary Hendrix, M. S., S. A. Graham, A. R. Carroll, E. R. Sobel, basins in China-Report of the American Sedimen- C. L. McKnight, B. J. Schulein, and Z. Wang, 1992, tary Basins Delegation to the People's Republic of Sedimentary record and climatic implications of China: United States Geological Survey Open-File recurrent deformation in the Tian Shan: evidence Report 86-327, 108 p. from Mesozoic strata of the north Tarim, south Carroll, A. R., Y. Liang, S. A. Graham, X. Xiao, M. S. Junggar, and Turpan basins, northwest China: GSA Hendrix, J. Chu, and C. L. McKnight, 1990, Junggar Bulletin, v. 194, p. 53-79. basin, northwest China: trapped late Paleozoic Jiang, Z., and M. G. Fowler, 1986, Carotenoid-derived ocean: Tectonophysics, v. 181, p. 1-14. alkanes in oils from northwestern China: Organic Carroll, A. R., 1991, Late Paleozoic tectonics, sedimen- Geochemistry, v. 10, p. 831-839. tation, and petroleum potential of the Junggar and King, D. J., J. Yang, and F. Pu, 1994, Thermal history of Tarim basins, northwest China: Ph.D. dissertation, the periphery of the Junggar basin, northwestern Stanford University, Stanford, California, 405 p. China: Organic Geochemistry, v. 21, p. 393-405. Carroll, A. R., S. C. Brassell, and S. A. Graham, 1992, Lawrence, S. R., 1990, Aspects of the petroleum geol- Upper Permian lacustrine oil shales, southern Jung- ogy of the Junggar basin, northwest China, in gar basin, northwest China: AAPG Bulletin, v. 76, J. Brooks, ed., Classic petroleum provinces: GSA p. 1874-1902. Publication no. 50, p. 545-557. Carroll, A. R., S. A. Graham, M. S. Hendrix, D. Ying, Lee, K. Y., 1985. Geology of the petroleum and coal and D. Zhou, 1995, Late Paleozoic tectonic amalga- deposits in the Junggar basin, Xinjiang Uygur mation of northwestern China: sedimentary record Zizhiqu, northwest China: United States Geological of the northern Tarim, northwestern Turpan, and Survey Open-File Report 85-230, 53p. southern Junggar basins: GSA Bulletin, v. 107, p. Liao, Z., L. Lu, N. Jiang, F. Xia, F. Sung, Y. Zhou, S. Li, 571-594. and Z. Zhang, 1987, Carboniferous and Permian in Carroll, A. R., 1998, Upper Permian organic facies evo- the western part of the east Tianshan mountains: lution, southern Junggar Basin, NW China: Organic Eleventh Congress of Carboniferous Stratigraphy Geochemistry, v. 28, p. 649-667. and Geology, Guide Book Excursion 4, 50 p. Clayton, J. L., J. Yang, J. D. King, P. G. Lillis, and Liu, S., 1993, Some Permian-Triassic Conchostracans A. Warden, 1997, Geochemistry of oils from the from the mid-Tianshan mts. of China and the signif- Junggar basin, northwest China: AAPG Bulletin, v. icance of their geological dating, in S. G. Lucas and 81, p. 1926-1944. M. Morales, eds., The Nonmarine Triassic: New Chen, Z., N. Wu, D. Zhang, J. Hu, H. Huang, G. Shen, Mexico Museum of Natural History & Science Bul- G. Wu, H. Tang, and Y. Hu, 1985, Geologic map of letin No. 3, p. 277-278. Permian Lacustrine Deposits of Northwest China 131

Nie, S., D. B. Rowley, R. Van der Voo, and M. Li, 1993, Wartes, M. A., A. R. Carroll, and T. J. Greene, 1999, Paleomagnetism of late Paleozoic rocks in the Tian- Permian sedimentary evolution of the Junggar and shan, northwestern China: Tectonics, v. 12, p. 568-579. Turpan-Hami basins, northwest China [abs.]: GSA Peng, X., and G. Zhang, 1989, Tectonic features of the Abstracts with Programs. Junggar basin and their relationship with oil and gas Watson, M. P., A. B. Hayward, D. N. Parkinson, and distribution, in K. J. Hsü, and X. Zhu, eds., Chinese Z. M. Zhang, 1987, Plate tectonic history, basin sedimentary basins: Amsterdam, Elsevier, p. 17-31. development and petroleum source rock deposition Shao, L., K. Stattegger, L. Wenhou, and B. J. Haupt, onshore China: Marine and Petroleum Geology, 1999, Depositional style and subsidence history of v. 4, p. 205-225. the Turpan Basin (NW China): Sedimentary Geol- XPGEG (Xinjiang Petroleum Geology Editing Group), ogy, v. 128, p. 155-169. 1991, Petroleum geology of China volume 15, part I, Sharps, R., Y. Li, M. McWilliams, and Y. A. Li, 1992, Junggar basin: Beijing Petroleum Industry Press, 390 p. Paleomagnetic investigations of Upper Permian Yang, J., L. Qu, H. Zhou, Z. Cheng, T. Zhou, J. Hou, sediments in the south Junggar basin, China: Jour- P. Li, S. Sun, Y. Li, Y. Zhang, X. Wu, Z. Zhang, and Z. nal of Geophysical Research, v. 97, p. 1753-1765. Wang, 1986, Permian and Triassic strata and fossil Tang, Z., J. Parnell, and A. H. Ruffell, 1994, Deposition assemblages in the Dalongkou area of Jimsar, Xin- and diagenesis of the lacustrine-fluvial Cangfang- jiang, Ministry of Geology and Mineral Resources gou Group (uppermost Permian to Lower Triassic), Geologic Memoir, Series 2, No. 3: Beijing, Geological southern Junggar basin, NW China: a contribution Publishing House, 262 p. (in Chinese with English from sequence stratigraphy: Journal of Paleolimnol- summary). ogy, v. 11, p. 67-90. Zhang, X., 1981, Regional stratigraphic chart of north- Tang, Z., J. Parnell, and F. J. Longstaffe, 1997a, Diagen- western China, branch of Xinjiang Uygur Autono- esis of analcime-bearing reservoir sandstones: the mous Region: Beijing, Geological Publishing House, Upper Permian Pingdiquan Formation, Junggar 496 p. (in Chinese). basin, northwest China: Journal of Sedimentary Zhao, B., 1982, The prospects of petroleum exploration Research, v. 67, p. 486-498. of Permo-Carboniferous in the Junggar Basin. Oil Tang, Z., J. Parnell, and F. J. Longstaffe, 1997b, Diagenesis and Gas Geology, v. 3, p. 1-14 (in Chinese with Eng- and reservoir potential of Permian-Triassic lish abstract). fluvial/lacustrine sandstones in the southern Junggar Zhao, X., Z. Lou, and Z. Chen, 1991, Response of allu- basin, northwestern China: AAPG, v. 81, p. 1843-1865. vial-lacustrine deposits of the Permian-Triassic Wartes, M. A., T. J. Greene, and A. R. Carroll, 1998, Cangfanggou Group to climate and tectonic regime Permian lacustrine paleogeography of the Junggar in Dalonggou, Junggar basin, Xinjiang, in K. R. and Turpan-Hami basins, northwest China: AAPG Kelts and C. Yang, eds., Comparative lacustrine Annual convention, Extended Abstracts, v. 2, sedimentation in China: Part 2, China Earth p. A682. Sciences, v. 1, p. 343-354.