Printer Friendly

Organic geochemistry of the Paleocene-Eocene oil shales of the Gongjue formation, Nangqian Basin, East-Central Tibetan Plateau.

1. Introduction

The Tibetan Plateau is referred to as the last frontier in petroleum exploration in China because it is located in the eastern part of the Tethyan Hydrocarbon Province, one of the most significant regions of hydrocarbon resources worldwide [1, 2]. For decades, numerous studies have focused on the sedimentary basins distributed across the "roof of the world", despite a number of challenges such as a complicated tectonic history and poor natural environmental conditions. In fact, some of these basins, like the Lunpola Basin [3, 4] and the Qiangtang Basin [5, 6], have proven to have promising prospects with industrial oil flow or oil shows.

The Nangqian Basin is located in the hinterland of the Tibetan Plateau. Previous research on the Nangqian Basin focused on the sedimentary characteristics of the basin fill [7-9], the basin's structural evolution [10], and potassium-rich volcanic rocks [11, 12]. However, a comprehensive study on the geochemistry of the oil shale of the Nangqian Basin has yet to be conducted. Oil shale deposits are widely distributed throughout several regions of China, with proven reserves of approximately 7199.37 x 108 tons (when converted to shale oil, approximately 476.44 x 108 t) [13]. The globally growing interest, especially in China, Estonia, Brazil and Australia, in oil shale over the past few decades has been related to its importance as a natural unconventional fuel resource that could be mined and converted to liquid fuel. In addition, the multi-purpose utilization of oil shale considering its energy potential and the minerals contained improves the competitiveness of the rock [14].

In this paper, we present the first organic geochemical data for oil shale from the Nangqian Basin, east-central Tibetan Plateau. The main objective of the study is to determine the type, proneness and maturity of organic matter, as well as the depositional environment of the shales in order to evaluate the hydrocarbon potential of the basin. We also aim at improving the understanding of the paleoenvironmental conditions during the deposition of the shale by using organic geochemical proxies.

2. Geological background

The Nangqian Basin, with an average elevation of over 4000 m, is a lacustrine-dominated Cenozoic sedimentary basin in the east-central Tibetan Plateau near the headwaters of the Lancangjiang River (also called the Mekong River). The NW-SE elongated basin is approximately 55 km long and 18 km wide [15]. The basin is situated in the middle part of the Qiangtang terrane, which is bounded by two major suture zones, the Jinshajiang Suture to the northeast and the Bangong-Nujiang Suture to the southwest (Fig. 1a).

The sedimentary basin fill is mainly composed of the Gongjue Formation, while the Nangqian Basin is similar to the nearby Gongjue Basin in terms of age, sedimentary fill and tectonic setting [17].

The Gongjue Formation of the Nangqian Basin, with a thickness of over 2000 m, unconformably overlies the Late Triassic strata. The measured sections A and B are located in the western margin of the Nangqian Basin (Fig. 1b). Based on the findings by Horton et al. [8] and our field observations, we divided the Gongjue Formation into three lithostratigraphic units (Fig. 2).

The oldest of the lithostratigraphic units (U1) is well exposed at Duriwa and Dongriga villages along the southwestern part of the basin. This unit comprises gray mudstone and marl with thin interbeds of oil shale, which suggests deposition in an offshore lacustrine environment. The organic-rich oil shale can be ignited directly. Palynomorph and ostracod assemblages are present in this unit and indicate that it is likely of Paleocene to Eocene age [18].

Unit 2 (U2) is very thick, over 1000 m, and is primarily composed of alluvial sandstone and medium- to thick-bedded, light gray to red, cobble-boulder conglomerate, which suggests that deposition occurred proximal to its source areas and may be related to tectonism during the Cenozoic Indo-Asian collision. The uppermost unit (U3) is a lacustrine deposit which consists of mudstone, minor carbonates, evaporite and volcanic rock. The volcanic rock is well known for its widespread deposition in the Qamdo-Nangqian area. The Middle-Upper Eocene tuffs of this unit have [sup.40]Ar/[sup.39]Ar ages of 37 to 38 Ma in the Nangqian Basin [10].

3. Materials and methods

A total of 11 outcrop oil shale samples were collected from section A of the Nangqian Basin (Fig. 2). The samples were collected after digging approximately 0.5 m into the subsurface and removing the uppermost layer to minimize the influence of surface weathering.

The samples were ground to analytical grain sizes (approximately 100 mg and 120 mesh) and dried at 60[degrees]C prior to further treatment. After the removal of carbonates by acidification using hydrochloric acid (HCl), a Leco CS-200 carbon-sulfur elemental analyzer was used to determine the total organic carbon (TOC) values. Rock-Eval pyrolysis was carried out on all of the samples using a Rock-Eval II instrument. The crushed samples were extracted with chloroform in a Soxhlet apparatus for 72 h. The obtained extracts are a measure of the amount of soluble organic matter (SOM). The asphaltenes were precipitated with petroleum ether, and then the deasphalted extracts were further separated by column chromatography into saturated hydrocarbons, aromatic hydrocarbons and NSO compounds by using a silica gel alumina column (500 mm x 10 mm ID, over 12 h).

The saturated hydrocarbon fractions were analyzed on an Agilent 6890 N gas chromatograph (GC) equipped with a 30 m x 0.20 mm fused silica column (0.2 [micro]m film). The oven was gradually heated from 70 to 300[degrees]C at a rate of 8[degrees]C/min, followed by an isothermal period of 20 min. An injection was performed in a split/splitless mode with an injector temperature of 300[degrees]C. Helium was used as the carrier gas.

The gas chromatography-mass spectrometry (GC-MS) analysis of saturates was completed using a TRACE2000/SSQ-7000 mass spectrometer connected to the gas chromatograph. Helium was used as the carrier gas, and a 30 m x 0.20 mm Varina CP Sil-8CB fused silica column (0.2 [micro]m film) was applied. The operating temperature was programmed from 80 to 160[degrees]C at a rate of 8[degrees]C/min and further to 310[degrees]C at 2.8[degrees]C/min, with a final isothermal hold at 310[degrees]C for 5 min.

Elemental analyses were performed on a FLASH EA-1112 Series elemental analyzer with an analytical precision of 0.3% for carbon and 0.5% for nitrogen [19].

All the experiments were performed at the Organic Geochemistry Laboratory, Institute of Exploration and Development, Huabei Oilfield Branch Company of China National Petroleum Corporation (CNPC).

4. Results and discussion

4.1. TOC, SOM and Rock-Eval

The TOC, SOM and Rock-Eval pyrolysis data for oil shale samples from the Gongjue Formation of the Nangqian Basin are summarized in Table 1. The TOC of the samples varies between 4.19 and 6.47 wt%, with the corresponding SOM values between 1193 and 2923 ppm. The Rock-Eval analysis of the bulk samples yielded hydrogen index (HI) values of 449 to 628 mg HC/g TOC. The hydrocarbon potential and free hydrocarbon content of the entire sample suite is indicated by parameters [S.sub.2] and [S.sub.1], respectively. The average [S.sub.1] and [S.sub.2] values are 2.96 and 30.04 mg HC/g rock, respectively (Table 1). The calculated parameter PY ([S.sub.1] + [S.sub.2]) is known as the potential yield and fluctuates between 28.30 and 42.43 mg HC/g rock.

4.2. Thermal maturity

Besides vitrinite reflectance (%[R.sub.o]), [T.sub.max] is another thermal stress parameter that can be used to estimate the thermal maturity of oil shale [20]. The [T.sub.max] values for the Nangqian oil shale samples are similar and relatively low, ranging from 413 to 421[degrees]C (Table 1). The calculated parameter [S.sub.1]/[S.sub.1] + [S.sub.2] is known as the production index (PI), which is also related to the stage of petroleum generation. For the samples the Rock-Eval [T.sub.max] is below 435[degrees]C, and PI less than 0.1 (except for sample NS7), suggesting that these are immature [4, 20].

Biomarkers hold information about the origin of organic matter but also record the level of maturity of the host sample. The moretane/hopane (M/H) ratio is sensitive to maturity because the former compound is thermally less stable than the latter [21-23], which allows the ratio to serve as a maturity indicator, especially for samples in the immature-early mature stage. Peters et al. [20] suggested that the M/H ratio near 0.8 indicates the immature stage, whereas M/H less than 0.15 is typical of the mature stage. Table 2 presents the M/H ratios for all of the analyzed samples. The relatively high M/H ratios (0.83 to 1.11) suggest that the Nangqian oil shale samples are immature. Furthermore, the degree of isomerization of biological markers, such as steranes and hopanes, is now widely applied to indicate the maturity of source rocks and petroleum. Isomerization at C-22 in C32 homohopane gives rise to the change of the 22S/(22S + 22R) ratio from zero to the equilibrium value, 0.57-0.62, during maturation [22]. The Nangqian oil shale samples have 22S/(22S + 22R) ratios between 0.29 and 0.47 (Table 2), while the fact that all these values remain below 0.57 suggests that the samples are mostly immature.

These maturity indicators are all related to the increasing maturity and can be correlated with each other. Overall, the assessed thermal maturity level based on the presented parameters implies that the samples are immature to early mature and are just entering the oil window.

4.3. Organic matter type and source

4.3.1. Elemental analysis of kerogen

The organic matter in sedimentary rocks possesses different characteristics and compositions due to the different types of sources. Traditionally, there are distinguished three types of kerogen: I, II and III, which on the Van Krevelen diagram show diverse evolution paths [24]. The elemental analysis data for the Nangqian oil shale samples are listed in Table 3. The atomic H/C and O/C ratios range from 1.44 to 1.58 and from 0.13 to 0.27, respectively. Typically, a cross-plot of H/C vs O/C is used to determine the kerogen type. Figure 3 shows that the organic matter in the studied samples is mainly of Type I or II.

4.3.2. Biomarkers

Gas chromatograms of the saturated hydrocarbons of selected Nangqian oil shale samples are shown in Figure 4, and the parameters of all samples are summarized in Table 2.

The extracts contain a wide range of n-[C.sub.15] to n-[C.sub.38] alkanes. The n-alkane distribution (Fig. 4) is dominated by middle- to long-chain (n-[C.sub.21+]) alkanes with an odd-over-even preference with high carbon preference index (CPI) values (2.23-4.14). Short-chain n-alkenes (n-[C.sub.21-]) composed of mixtures of n-[C.sub.15], n-[C.sub.17] and n-[C.sub.19] are derived from algal and zooplanktonic sources, whereas the higher plants are prone to produce long-chain n-alkenes [25]. The much greater concentrations of n-[C.sub.27], n-[C.sub.29] and n-[C.sub.31] alkanes, compared with n-[C.sub.15], n-[C.sub.17] and n-[C.sub.19] homologues, are typical of higher land plants [26].

The mass chromatograms (m/z 217, m/z 191) in Figure 5 depict the distribution of regular steranes and hopanes, respectively, and Table 2 lists the relative proportions of [alpha][alpha][alpha] (R) steranes.

The high proportion of [C.sub.27] steranes indicates the planktonic origin of organic matter, whereas the dominance of [C.sub.29] points to the input of terrigenous organic material; hence, the composition of steranes could be used to identify the OM source [27, 28]. The samples have a higher proportion of [C.sub.27] sterane (48-54%) compared to [C.sub.29] (21-37%) and C28 (15-28%) homologues (Table 2), which gives evidence of a major contribution of aquatic algal-bacterial sources with considerable terrigenous organic matter input, as illustrated by the distribution of steranes (Fig. 6a) and a higher proportion of the short-chain n-alkanes.

Based on the distribution of steranes, the abundance of wax n-alkanes with a marked odd carbon number predominance, as well as high atomic H/C ratios, we propose a mixed source with both aquatic and terrigenous organic input.

4.4. Hydrocarbon potential

Usually, outcrop samples have been somewhat affected by long-term weathering, especially for the rocks from the Tibetan Plateau. In addition, the evaluation criteria of the hydrocarbon source rock are different depending on rock type and the location of the study area [4]. Nevertheless, the oil shale from the lower part of the Gongjue Formation of the Nangqian Basin, with high TOC, PY and HI, is considered to be a high quality source rock, according to the evaluation criteria of the hydrocarbon source rock in the Qiangtang Basin of the Tibetan Plateau [29, 30]. Oil shale samples from the Gongjue Formation are characterized by relatively low maturity and their kerogen type is mostly II. Therefore, if subjected to appropriate burial and heating, the hydrocarbon potential of the Gongjue Formation may be sufficient to generate liquid hydrocarbons. However, due to the current insufficient exploration, poor natural environmental conditions and lack of necessary facilities, the economic utilization of this oil shale is quite impossible. At the same time, Tertiary lacustrine oil shales are widely spread in the interior of the Tibetan Plateau, especially in the basins of central Tibet (e.g., Lunpola and Qiangtang). So, utilization of the Gongjue Formation oil shale might be possible if development and exploitation is carried out concurrently with the respective activities in the adjacent basins.

4.5. Depositional environment

Acyclic isoprenoids occur in significant amounts in all of the studied oil shale samples. The pristane-to-phytane ratios are listed in Table 2. In all the samples, the Ph content is higher than that of Pr, giving Pr/Ph ratios between

0.10 and 0.23. The Pr/Ph ratio reflects redox conditions during deposition of the source rock [31, 32]. However, Ten Haven et al. [33] argue that the Pr/Ph ratio cannot be used as an indicator of oxygen levels. Peters et al. [20] have suggested that Pr/Ph < 0.8 indicates saline to hypersaline conditions associated with the deposition of evaporite and carbonates. Constructed on the basis of the ratios of isoprenoids and n-alkanes, the ternary diagram in Figure 6b implies the deposition of oil shale in a salt lake, further justifying the use of the Pr/Ph ratio as a proof of paleo-lake conditions [34].

Gammacerane, which is considered to be an indicator of reducing and hypersaline conditions [35-36] or associated with a stratified water column [37], is abundant in all of the oil shale samples studied (Fig. 5b). The high gammacerane index, 1.84-3.27 (Table 2), is consistent with the interpretation of low Pr/Ph ratios, reflecting a saline to hypersaline setting associated with evaporate and carbonates deposition.

5. Conclusions

Oil shale samples from the lower part of the Gongjue Formation in the Nangqian Basin were analyzed for geochemical characteristics, paleo-lake deposition conditions and organic matter source. Based on the results of analysis the following conclusions can be drawn:

1. The oil shale samples have high values of TOC (4.17-6.47 wt%), SOM (1193-2923 ppm), PY (28.30-42.43 mg HC/g rock) and HI (449-628 mg HC/g TOC), which gives evidence of a good hydrocarbon generation potential of Nangqian oil shale.

2. The Rock-Eval pyrolysis and biomarker data of the samples confirm maturities in the pre- to early stages of oil generation.

3. Elemental analysis and pyrolysis data show that the organic matter of Nangqian oil shale mostly originates from lacustrine algae. However, based on the odd-over-even carbon number predominance of n-alkanes and high proportions of long-chain n-alkanes, there may be observed a strong terrestrial source signal.

4. The gammacerane index of 1.84-3.27 and high concentrations of phytane (Pr/Ph < 0.23) reveal that the Nangqian oil shale is associated with a restricted, saline depositional setting and might have had a stratified water column.

doi: https//


This research was financially supported by the China Geological Survey (Nos. 121201010000150010-01 and 1212011220800) and the National Natural Science Foundation of China (No. 41572188). We thank Xiaohan Li, Peng Zuo, Wei Sheng, Bo Wang for the fieldwork, and Dr. Shunping Ma for assistance in the lab. We also thank Prof. Dujie Hou for helpful comments on the early version of the manuscript. Special thanks go to Meelika Nomme, Riina Suld and the anonymous reviewers for the extremely useful and constructive comments on the manuscript.


[1.] Wang, C., Zhang, S. Preliminary analysis of petroliferous basins and oil-gas prospects in Qinghai-Xizang (Tibet) plateau. Earth Science, 1996, 21, 120-129 (in Chinese with English abstract).

[2.] Klemme, H. D., Ulmishek, G. F. Effective petroleum source rocks of the world: stratigraphic distribution and controlling depositional factors. Am. Assoc. Petr. Geol. B, 1991, 75(12), 1809-1851.

[3.] Gu, Y., Shao, Z., Ye, D., Zhang, X., Lu, Y. Characteristics of source rocks and resource prospect in the Lunpola Basin, Tibet. Petroleum Geology & Experiment, 1999, 21, 340-345 (in Chinese with English abstract).

[4.] Han, Z., Xu, M., Li, Y., Wei, Y., Wang, C. Paleocene-Eocene potential source rocks in the Avengco Basin, Tibet: Organic geochemical characteristics and their implication for the paleoenvironment. J. Asian Earth Sci., 2014, 93, 60-73.

[5.] Fu, X., Wang, J., Zeng, Y., Li, Z., Wang, Z. Geochemical and palynological investigation of the Shengli River marine oil shale (China): Implications for paleoenvironment and paleoclimate. Int. J. Coal Geol., 2009, 78(3), 217-224.

[6.] Yang, R., Cao, J., Hu, G., Fu, X. Organic geochemistry and petrology of Lower Cretaceous black shales in the Qiangtang Basin, Tibet: Implications for hydrocarbon potential. Org. Geochem., 2015, 86, 55-70.

[7.] Zhou, J., Wang, J., Yin, A., Spurlin, M. S., Horton, B. K. Depositional patterns and tectonic setting of early Tertiary basins in the NE margin of the Tibetan Plateau: A case study of the Nangqian and Xialaxiu basins. Acta Sedimentologica Sinica, 2002, 20(1), 85-91 (in Chinese with English abstract).

[8.] Horton, B. K., Yin, A, Spurlin, M. S., Zhou, J, Wang, J. Paleocene-Eocene syncontractional sedimentation in narrow, lacustrine-dominated basins of east-central Tibet. Geol. Soc. Am. Bull., 2002, 114(7), 771-786.

[9.] Du, H., Jiang, Y, Yan, Z., Hou, Z., Yang, T., Guo, F., Yang, Q. Sedimentary characteristics and environment of the Paleogene Nangqian basin in Qianghai Province. Acta Geologica Sinica, 2011, 85, 383-395 (in Chinese with English abstract).

[10.] Spurlin, M. S., Yin, A., Horton, B. K., Zhou, J., Wang, J. Structural evolution of the Yushu-Nangqian region and its relationship to syncollisional igneous activity, east-central Tibet. Geol. Soc. Am. Bull., 2005, 117(9/10), 1293-1317.

[11.] Deng, W., Sun, H., Zhang, Y. Petrogenesis of Cenozoic potassic volcanic rocks in Nangqian Basin. Chinese Journal of Geology, 2001, 36(3), 304-318 (in Chinese with English abstract).

[12.] Zhu, L., Zhang, H., Wang, J., Zhou, J., Xie, G. [sup.40]Ar/[sup.39]Ar chronology of high-K magmatic rocks in Nangqian basins at the northern segment of the Jinsha-Red River shear zone. Geotectonica et Metallogenia, 2006, 30, 241-247 (in Chinese with English abstract).

[13.] Chen, M., Cheng, Y., Li, W. Exploitation and utilization of oil shale in the coal measure strata of the Haishiwan mine, Yaojie coalfield, China. Oil Shale, 2015, 32(4), 335-355.

[14.] Brendow, K. Global oil shale issues and perspectives (Synthesis of the Symposium on Oil Shale held in Tallinn (Estonia) on 18 and 19 November 2002). Oil Shale, 2003, 20(1), 81-92.

[15.] Yang, D., Wang, P. The determinations of plateau age by [sup.40]Ar/[sup.39]Ar dating on Cenozoic calc-alkalic trachytes of Nangqen Basin, northern transverse mountains. In: Contribution to the Geology of the Qinghai-Xizang (Tibet) Plateau. Geological Publishing House, Beijing, 1988, 19, 9-44 (in Chinese with English abstract).

[16.] Deng, J., Wang, Q., Li, G., Santosh, M. Cenozoic tectono-magmatic and metallogenic processes in the Sanjiang region, southwestern China. Earth-Sci. Rev, 2014, 138, 268-299.

[17.] Tibet BGMR [Tibet Bureau of Geology and Mineral Resources]. Geologic map of the Nangqian, Changdu, Jiangda region, with geologic report (1:250 000 scale), 2007.

[18.] Wei, M. Eogene ostracods from Nangqen in Qinghai. In: Contribution to the Geology of the Qinghai-Xizang (Tibet) Plateau. Geological Publishing House, Beijing, 1985, 17, 313-324 (in Chinese with English abstract).

[19.] Wang, L., Wang, C., Li, Y., Zhu, L., Wei, Y. Sedimentary and organic geo-chemical investigation of tertiary lacustrine oil shale in the central Tibetan plateau: Palaeolimnological and palaeoclimatic significances. Int. J. Coal Geol., 2011, 86(2), 254-265.

[20.] Peters, K. E., Walters, C. C., Moldowan, J. M. The Biomarker Guide Volume 2: Biomarkers and Isotopes in Petroleum Exploration and Earth History, 2nd ed. Cambridge University Press, 2005.

[21.] Ten Haven, H. L., De Leeuw, J. W., Sinninghe Damste, J. S., Schenck, P. A., Palmer, S. E., Zumberge, J. E. Application of biological markers in the recognition of palaeohypersaline environments. Geol. Soc. Spec. Publ., 1988, 40, 123-130.

[22.] Seifert, W. K., Moldowan, J. M. The effect of thermal stress on source-rock quality as measured by hopane stereochemistry. Phys. Chem. Earth, 1980, 12, 229-237.

[23.] Kara-Gulbay, R., Korkmaz, S. Occurrences and origin of oils and asphaltites from South East Anatolia (Turkey): Implications from organic geochemistry. J. Petrol. Sci. Eng., 2012, 90, 145-158.

[24.] Tissot, B., Durand, B., Espitalie, J., Combaz, A. Influence of nature and diagenesis of organic matter in formation of petroleum. Am. Assoc. Petr. Geol. B., 1974, 58(3), 499-506.

[25.] Grimalt, J., Albaiges, J. Sources and occurrence of [C.sub.12]-[C.sub.22] n-alkane distributions with even carbon-number preference in sedimentary environments. Geochim. Cosmochim. Ac., 1987, 51(6), 1379-1384.

[26.] Bourbonniere, R. A., Meyers, P. A. Sedimentary geolipid records of historical changes in the watersheds and productivities of Lakes Ontario and Erie. Limnol. Oceanogr., 1996, 41(2), 352-359.

[27.] Seifert, W. K., Moldowan, M. J. Applications of steranes, terpanes and monoaromatics to the maturation, migration and source of crude oils. Geochim. Cosmochim. Ac., 1978, 42(1), 77-95.

[28.] Huang, W., Meinschein, W. G. Sterols as ecological indicators. Geochim. Cosmochim. Ac., 1979, 43(5), 739-745.

[29.] Ding, W., Wan, H., Zhang, Y., Han, G. Characteristics of the Middle Jurassic marine source rocks and prediction of favorable source rock kitchens in the Qiangtang Basin of Tibet. J. Asian Earth Sci, 2013, 66, 63-72.

[30.] Wang, J., Ding, J., Wang, C., Tan, F. Investigation and Assessment of Oil and Gas Resources in the Tibetan Plateau. Geological Publishing House, Beijing, 2009 (in Chinese).

[31.] Powell, T. G., McKirdy, D. M. Relationship between ratio of pristane to phytane, crude oil composition and geological environment in Australia. Nature, 1973, 243, 37-39.

[32.] Didyk, B. M., Simoneit, B. R. T., Brassell, S. C., Eglinton, G. Organic geo-chemical indicators of palaeoenvnonmental conditions of sedimentation. Nature, 1978, 272, 216-222.

[33.] Ten Haven, H. L., De Leeuw, J. W., Rullkotter, J, Sinninghe Damste, J. S. Restricted utility of the pristane/phytane ratio as a palaeoenvironmental indicator. Nature, 1987, 330, 641-643.

[34.] Wang, T., Zhong, N., Hou, D., Bao, J., Huang, G., Li, X. Several genetic mechanisms of immature crude oils in China. Acta Sedimentologica Sinica, 1997, 15(2), 75-83 (in Chinese with English abstract).

[35.] Moldowan, J. M., Seifert, W. K., Gallegos, E. J. Relationship between petroleum composition and depositional environment of petroleum source rocks. Am. Assoc. Petr. Geol. B., 1985, 69(8), 1255-1268.

[36.] Fu, J., Sheng, G., Peng, P., Brassell, S. C., Eglinton, G., Jiang, J. Peculiarities of salt lake sediments as potential source rocks in China. Org. Geochem., 1986, 10(1), 119-126.

[37.] Sinninghe Damste, J. S., Kenig, F., Koopmans, M. P., Koster, J, Schouten, S., Hayes, J., De Leeuw, J. W. Evidence for gammacerane as an indicator of water column stratification. Geochim. Cosmochim. Ac., 1995, 59(9), 1895-1900.

Presented by K. Kirsimae

Received May 22, 2016


(a) School of Earth Science and Resources, China University of Geosciences, Beijing 100083, China

(b) Research Center of Tibetan Plateau Geology, China University of Geosciences, Beijing 100083, China

(c) Research Institute of China National Offshore Oil Corporation, Beijing 100027, China

(d) Oil & Gas Survey, China Geological Survey, Beijing 100029, China

* Corresponding author: e-mail;

Caption: Fig. 1: (a) Simplified tectonic map of the study area and the adjacent region, including suture zones and major rivers (modified from [16]). Abbreviations: AKMS--Anyimaqin-Kunlun-Muztagh Suture, JS--Jinshajiang Suture, BNS Bangong-Nujiang Suture, ITS--Indus-Tsangpo Suture; (b) simplified geological map of the Nangqian Basin. Locations of the measured sections A and B are marked. Abbreviations: J--Jurassic, T--Triassic, P--Permian, C--Carboniferous.

Caption: Fig. 2: Lithology log of sediments of the Nangqian Basin (based on [8] and our observations) and measured sections (sections A and B), including the location of the studied samples and age controls based on [8, 18].

Caption: Fig. 3: Cross-plot of H/C vs O/C atomic ratios of the analyzed Nangqian oil shale samples showing the type of kerogen.

Caption: Fig. 4: Gas chromatograms of the saturated fractions of selected Nangqian oil shale samples.

Caption: Fig. 5: Mass chromatograms for a representative oil shale sample NS7 showing the distribution of (a) steranes (m/z 217) and (b) hopanoids (m/z 191).

Caption: Fig. 6: (a) Ternary diagram of [alpha][alpha][alpha](H)-20R steranes ([C.sub.27], [C.sub.28], [C.sub.29]) showing the source of organic matter in the studied oil shale samples (after [28]); (b) ternary diagram of Pr/Ph, Ph/n-[C.sub.18] and Pr/n-[C.sub.17] ratios showing the depositional conditions of the samples (after [34]).
Table 1. TOC, SOM and Rock-Eval pyrolysis data and
calculated parameters for outcrop oil shale samples
from the Gongjue Formation in the Nangqian Basin

Sample No.   TOC, wt%   SOM, ppm   [T.sub.max],    [S.sub.1],
                                    [degrees]C    mg HC/g rock

NS1            4.19       1193         419            2.13
NS2            5.07       1740         421            2.61
NS3            5.18       1421         421            2.47
NS4            4.26       2149         419            2.61
NS5            4.66       1668         418            2.63
NS6            6.47       2923         420            3.66
NS7            5.35       2051         414            3.40
NS8            5.93       2189         414            2.98
NS9            6.03       2516         416            3.62
NS10           5.36       2419         420            3.23
NS11           4.97       2434         413            3.22

Sample No.    [S.sub.1],     PY, mg      HI, mg     PI
             mg HC/g rock   HC/g rock   HC/g TOC

NS1             26.17         28.30      625.25    0.08
NS2             31.81         34.43      627.73    0.08
NS3             31.07         33.53      599.83    0.07
NS4             26.38         28.99      619.00    0.09
NS5             26.73         29.36      573.90    0.09
NS6             38.76         42.43      599.24    0.09
NS7             28.37         31.77      530.03    0.11
NS8             26.62         29.60      449.21    0.10
NS9             33.55         37.17      556.08    0.10
NS10            33.10         36.33      617.61    0.09
NS11            27.94         31.16      562.44    0.10

Note: SOM--soluble organic matter; PY--potential yield
([S.sub.1] + [S.sub.2]); HI--hydrogen
index ([S.sub.2] x 100/TOC); PI--production index
[[S.sub.1]/([S.sub.1] + [S.sub.2])].

Table 2. Geochemical parameters for organic extracts
of Nangqian oil shale samples

Sample No.    Pr/Ph    Pr/n-[C.sub.17]    Ph/n-[C.sub.18]    CPI

NS1            0.11          0.13               8.16         4.03
NS2            0.10          0.11               4.89         2.94
NS3            0.12          0.15               8.58         4.14
NS4            0.11          0.10               8.63         3.88
NS5            0.11          0.12               8.42         3.82
NS6            0.20          0.49               2.12         2.78
NS7            0.19          0.46               1.62         2.23
NS8            0.15          0.35               1.66         2.15
NS9            0.20          0.49               2.24         3.04
NS10           0.19          0.46               2.89         3.24
NS11           0.20          0.47               3.01         3.21

Sample No.    GI     22S/(22S + 22R)    M/H

NS1           3.27         0.43         1.03
NS2           2.90         0.47         0.87
NS3           2.89         0.42         0.98
NS4           2.97         0.45         0.89
NS5           3.01         0.43         0.93
NS6           1.84         0.29         1.11
NS7           1.96         0.39         0.83
NS8           2.15         0.42         0.90
NS9           1.96         0.33         1.11
NS10          1.96         0.35         1.08
NS11          2.07         0.35         1.00

Sample No.    [C.sub.27]%    [C.sub.28]%    [C.sub.29]%

NS1                49             15             36
NS2                50             15             35
NS3                51             15             34
NS4                49             16             35
NS5                48             15             37
NS6                53             25             22
NS7                49             28             23
NS8                52             22             26
NS9                52             27             21
NS10               53             21             26
NS11               50             27             23

Note: Pr--pristane; Ph--phytane; CPI--carbon
preference index; GI--gammacerane index =
gammacerane/[[C.sub.31] hopane(22S + 22R)/2];
22R/(22S + 22R) - 22R/(22S + 22R) homohopane
(for [C.sub.32]); m/h--moretane/hopane (for
[C.sub.30]); [C.sub.27]% - [C.sub.27][alpha][alpha][alpha](R)/
[C.sub.27]-[C.sub.29][alpha][alpha][alpha](R) steranes;
[C.sub.28]% - [C.sub.28][alpha][alpha][alpha](R)/
[C.sub.27]-[C.sub.29][alpha][alpha][alpha](R) steranes;
[C.sub.29]% - [C.sub.29][alpha][alpha][alpha](R)/
[C.sub.27]-[C.sub.29][alpha][alpha][alpha](R) steranes.

Table 3. The results of elemental analysis
of Nangqian oil shale samples

Sample No.   C, %    H, %   O, %    H/C    O/C

NS1          56.18   6.73   11.44   1.44   0.15
NS2          56.58   7.09   10.01   1.50   0.13
NS3          58.43   7.46   10.45   1.53   0.13
NS4          56.51   7.24   9.57    1.54   0.13
NS5          56.91   7.30   9.75    1.54   0.13
NS6          57.03   7.34   10.11   1.55   0.13
NS7          55.51   7.17   9.74    1.55   0.13
NS8          53.60   6.94   9.09    1.55   0.13
NS9          58.01   7.52   9.85    1.56   0.13
N4S10        31.53   3.63   8.96    1.38   0.21
NS11         30.04   3.70   10.83   1.48   0.27
COPYRIGHT 2017 Estonian Academy Publishers
No portion of this article can be reproduced without the express written permission from the copyright holder.
Copyright 2017 Gale, Cengage Learning. All rights reserved.

Article Details
Printer friendly Cite/link Email Feedback
Author:Qi, Zhaolin; Li, Yalin; Wang, Chengshan; Sun, Tao; Zhang, Jinhu
Publication:Oil Shale
Article Type:Report
Geographic Code:9CHIN
Date:Mar 1, 2017
Previous Article:Geopolymeric potential of the Estonian oil shale solid residues: petroter solid heat carrier retorting ash.
Next Article:Characteristics and resource potential of oil shale in China.

Terms of use | Privacy policy | Copyright © 2019 Farlex, Inc. | Feedback | For webmasters