Organic Geochemical Characteristics of Mudstone and Marl from Western Hoh Xil Basin of Tibet

Key Laboratory of Western China’s Mineral Resources of Gansu Province, Lanzhou University, Lanzhou 730000, China State Key Laboratory of Oil and Gas Reservoir Geology and Exploitation (Chengdu University of Technology), Chengdu 610059, China School of Mines, Inner Mongolia University of Technology, Hohhot 010051, China Key Laboratory of Geoscience Spatial Information of Land and Resources, Chengdu 610059, China Geomathematics Key Laboratory of Sichuan Province, Chengdu 610059, China Department of Civil Engineering, Ordos Institute of Technology, Ordos 017000, China Department of Geology, Northwest University, Xian 710069, China


Introduction
After years of geological investigation, the Hoh Xil basin was considered to be one of the important targets of hydrocarbon resource exploration for continental basin of Tibetan Plateau. We found two continental facies oil and gas Cenozoic basin belts of Bangong-Nujiang and Jinsha River on Tibetan Plateau. These basins had good prospects for preserving oil and gas resources and exploration potential. The discovery of crude oil from Lunpola basin confirmed that reservoirs of fossil resources occurred in Qinghai-Tibet plateau [1,2]. And the Hoh Xil basin has been confirmed existing a better prospect for preserving oil and gas too [3][4][5]. The eastern basin and western basin (Yanghu basin) of Hoh Xil had a conjoined basement, and there existed a unified Hoh Xil basin in Miocene [6][7][8]. Because of complex tectonism, the geological survey of western basin was very few. Understanding the geological survey of the western Hoh Xil basin (WHXB) is very important to recognize the overall situation of Cenozoic basins on Tibetan Plateau and the plateau lifting. Recently, sedimentary rocks of Wudaoliang Group in Miocene were discovered in WHXB. In this paper, we carried out detailed organic geochemistry investigations of these rocks in WHXB. The pivotal aim is to analyze paleoenvironment and paleoclimatic changes, to give the other geologists more information of Tibet.

Geological Setting
Hoh Xil basin is located in north Qiangtang block and the central of Bayankala block, crossing the suture of Jinsha River, and it is the greatest Cenozoic continental basin in Tibet [4,9]. The western Hoh Xil basin (WHXB), near the eastern basin of Hoh Xil (EHXB), is an uncivilized basin in the central Tibetan Plateau [7,10,11] (Figure 1). Because of the harsh geographical environment and high altitude, the geology of the WHXB remains indeterminate. The work focuses on the detrital organic geochemical investigation in WHXB ( Figure 1).
The west basin of Hoh Xil is located at an altitude of more than 4000 m with the area of 28,000 km 2 , which belongs to the depopulated zone of Tibet province. It is bounded in the south of eastern Kunlun mountains and in the east of the Altyn mountains. The length of WHXB is about 540 km, and the width is about 60 km. In the west, the basin is near to Altyn sinistral strike-slip faults with its south branch. In the north, it is near to Subashi-Muztagh-Whale Lake fault zone, and it is adjacent to the microcontinental block of Kunlun. The south boundary of the basin is Lazhulong-Xijin Ulan-Jinsha fault zone, which is adjacent to the Qiangtang terrane.
The geological investigation revealed that the outcropping strata in WHXB were mainly Devonian, Permian, Triassic, Jurassic, Paleogene, and Neogene. A set of purple continental clastic rocks and carbonate of Cenozoic strata occurred in WHXB too. The Cenozoic sedimentary sequences contain three main parts in these strata of Wudaoliang Group, Fenghuoshan Group, and Yaxicuo Group. At the bottom of EHXB, the Fenghuoshan Group contains sandstone, bioclastic limestone in lacustrine, and fluvial, rounded conglomerate, which obtains the magnetostratigraphic age during the Early Eocene to Early Oligocene (31.3-52.0 Ma) [12]. The Fenghuoshan Group was covered by the Yaxicuo Group (Early Oligocene). The Yaxicuo Group comprises fluvial and playa gypsum, marl, mudstone, and sandstone in Oligocene (23.8-31.3 Ma) [8]. The uncomfortably overlying strata of the uppermost unit (Wudaoliang Group) consist mainly of oil shale, mudstone, and lacustrine marl with biostratigraphical age of basement about~22 Ma [8]. The clastic rock association of Shapoliang (P01) in WHXB is consistent with the lithologic association of the Yaxicuo Group of Oligocene in EHXB; both of them uncomfortably underlie the volcanic rock of Chabaoma Formation [13]. And lacustrine carbonate of Fengcaogou (P02) in WHXB is consistent with the lithologic association of Wudaoliang Group in EHXB; both of them to belong to Miocene with nearly horizontal occurrence. In the south of EHXB, there is a huge south poured Paleogene thrust system, which is connected with the Tanggula thrust system of south WHXB. Shapoliang (P01) and Fengcaogou (P02) sections were measured at the marginal southeast of the WHXB in the geological survey. Two sections have the relationship of superposing; the profiles have been measured from the core of the syncline to the south part, no bottom. The top of profiles contacts with the Triassic through the fault.

Sedimentary Characteristics
Detrital zircon U-Pb isotopic compositions, sedimentary facies, and deformation of Shapoliang and Fengcaogou sections in WHXB are similar with the Oligocene Yaxicuo Formation and Miocene Wudaoliang Group of EHXB, respectively [7]. There are two depositional sequences developed in WHXB, including the lower alluvial fan (Shapoliang section) and upper lacustrine facies (Fengcaogou section), with a total thickness exceeding 1302 m. The Wudaoliang Group comprised crystalline limestone, bioclastic limestone, algal lump limestone, calcarenite, and marl in EHXB with the characteristics of carbonate of a paleolake [4]. The research section of Wudaoliang Group (Fengcaogou section, P02) is located in the southeast part of the WHXB (Figure 2).
In the low part of P02 of Wudaoliang Group, the unit contains gray, yellow-gray, gray-green, and gray-black mudstone and silty mudstone. This unit is sandwiched into maroon thin-middle layer of mudstone, argillaceous siltstone, silty mudstone, and fine sandstone; and some graygreen sheet marl and sandy limestone are outcrop. In the middle part, lithologic column contains the interbedded fine siltstone, mudstone, gray marl, and sandy limestones; this unit was sandwiched into thickness marls (up to 3.0 m). The upper part shows the gray marl, yellow fine sandstone, and brown red silty mudstone with a coarsening-upward sequence from bottom to top, which deposits marl-silty mudstone in the lower part and fine sandstone-siltstone in the upper part ( Figure 3). This section presents a sedimentary cycle with coarsening-upward in the overall. Potential organic rocks occur in lower-middle part of Fengcaogou section, which is made up of gray and yellow-gray mudstone, gray-black mudstone, and gray-green marl with a thickness of about 100 m.
The sedimentary environment of Wudaoliang Group belongs to the shallow lacustrine [14]. The Fengcaogou section mainly contains marl, sandstone, siltstone, and mudstone with the thickness of about 205 m. The lithofacies indicate the depositional environment is lacustrine. The massive argillaceous rocks of the Fengcaogou section need suspension in a peaceful water environment. According to characteristics of deposition of profiles, the Fengcaogou section of Wudaoliang Group experienced the evolution of depositional environment by semideep to shallow lake subfacies.

Research Methods
4.1. Sample. 20 samples are selected from the Fengcaogou profile in the western Hoh Xil basin. All of the samples were analyzed by geochemical methods. Details of sampling location, lithologic association, and stratigraphic columns are shown in Figure 3. In order to minimize the modern pollutions on surface and the effects of biodegradation and weathering, we used a shovel to collect fresh samples. After the collection of samples from the measured profiles systematically, organic geochemical tests were conducted. There are distinctive heterogeneities in the deposition of lacustrine sedimentary rocks (Table 1). After the evaluation of 2 Geofluids Wudaoliang Group samples in the WHXB, gray or yellowgray mudstones belong to nonpoor organic types of rocks; gray-black mudstones belong to good organic types of rocks; gray-green marl is moderate-good organic types of rocks. The types of organic matter in mudstone belong to types II and III. The types of OM in marl belong to type I-II 1 .

Analytical
Methods. Some rocks are prepared to the test of organic petrology, Rock-Eval pyrolysis, TOC, and δ 13 C. Saturated fractions of some samples are tested by the method of GC and GC-MS. Total organic carbon is analyzed using the equipment Leco CS-200 carbon-sulfur. After getting rid of carbonate by hydrochloric acid (HCl), some sample (120 mesh and 100 mg) was raising temperature to 1200°C in the induction furnace. The test of Rock-Eval pyrolysis was conducted on a TOC module-equipped apparatus with Rock-Eval II by strict procedures [15]. In the Soxhlet apparatus, some samples were conducted with chloroform for 72 h. After setting of asphaltenes, through a silica gel alumina column, NSO compounds, saturated hydrocarbons, and aromatic hydrocarbons were isolated from extracts by column chromatography [16]. GC-MS testing of saturated hydrocarbon is conducted using a Finnigan SSQ-7000 spectrometer. This instrument equipped is with DB5-MS fused silica capillary column (0:32 mm ID × 30 m × 0:25 μm film thickness). Carrier gas is helium. The oven is isothermally kept at 35°C in 1 min, then raised to 120°C by 10°C/min, and then increased to 300°C by 3°C/min, keeping this temperature for half an hour. MS is conducted by MID on a source temperature at 200°C with ionization energy of 70 eV. To identify molecular fossils, metastable ion transition for tricyclic terpanes and hopanes (m/z 191) and steranes (m/z 217) was kept an account of a periodic time of 1 s and a residence time for 25 ms per ion [17].
HCI/HF method is applied to 20 samples for kerogen isolation. First, rock fragments were leached in 12 N HCl for getting rid of carbonates in 12 h, and then, keep them clean with distilled water. Second, samples were conducted by hydrofluoric acid to get rid of silicate in 12 h [18]. Third, samples used distilled water for cleaning. Then, samples were again leached with 12 N HCl [18]. Maceral content is conducted by Zeiss Axioskop 2 plus microscope and a point counter for visual evaluating [16]. The test of N, C, H, S, and O was conducted using a FLASH EA-1112 instrument; the accuracy is 0.5% for N and 0.3% for C. The determination of δ 13 C kerogen is conducted using the EA Finnigan Delta plus XL mass spectrometer; precision of carbon isotope is ±0.2‰ [19]. Isotopic analyses and GC-MS analyses as well as others analyses were carried out in the Organic Geochemistry Laboratory of Huabei Oilfield Branch Company of PetroChina.  Table 1. TOC content of Fengcaogou mudstones is in the range of 0.03-1.38 wt.% and an average of 0.19% with most samples > 0:1 wt:%. After the recovery with coefficient of 2.2 [20], the restoration of organic carbon content is in the range of 0.08%~3.04 wt.% and an average of 0.42%. The TOC content of the Fengcaogou marl is in the range of 0.09~0.18 wt.% and an average of 0.14%; after the recovery with coefficient of 1.5 [20], the restoration of organic carbon content is in the range of 0.13%~0.27 wt.% and an average of 0.20%.

Results and Discussion
Maceral composition of kerogens from the Fengcaogou section is shown in Table 2. Amorphous organic matter exhibits a high abundance ranging from 50% to 90% with an average of 66%. Exinite is in the range of 0~15 wt.% and an average of 4.37%. Vitrinite is in the range of 3~22 wt.% and an average of 16.6%. Inertinite is in the range of 5~31 wt.% and an average of 12.95%. Organic matter of kerogen in mudstone shows the types of mixed II (II 1 -II 2 ), whereas kerogen in marl shows the types of I-II 1 .
Rock-Eval S 1 and S 2 are in the change of 0.02-0.24 and 0.06-1.17 mg HC/g rock. S 2 values of marl are in range of 0.09-0.19 mg HC/g rock, compared with 0.06-0.15 mg HC/g rock for mudstone (except P02-5S4) ( Table 1). The value of PY changes from 0.09 to 1.41 mg HC/g rock, which can reflect the potential yield and inversion of OM [21]. HI values are not high with the range of 50 to 200 mg HC/g TOC. The HI of marls is higher with the value of 89 to 144 mg HC/g TOC. Ro values change from 0.55 to 0.73. The color of sapropel group in kerogen (yellow) reflects that OM belongs to immature to early mature.
T max of all samples changes from 370°C to 532°C with the average of 437°C (Table 1). In the mudstone, 9 samples of T max values < 435°C indicating a thermally immature stage; 3 samples of T max values change from 435°C to 440°C at low mature stage; 4 samples of T max are between 450°C and 580°C at high mature stage. Organic matter of mudstones is in immaturity-low maturity stage. T max values of marl change from 426 to 447°C; these indicate thermally immature-mature. Difference in thermal maturity of two rocks may depend on the history of burial. The PI (production index) values of all samples are from 0.11 to 0.33. The maturity suggested by PI and T max are not completely consistent, which may be due to the weathering [22].  4 Geofluids

Characteristics of the Element and Kerogen.
The characteristics of element can reflect the chemical features of isolated kerogen [23]. And the analysis results of element are shown in Table 2 Figure 4), which suggest the probable input of allochthonous OM. And kerogens of type I with lacustrine source are input by AOM and planktonic algae [24]. The variation tendency in different lithology is consistent with kerogen's maceral composition. AOM make up 75-90% kerogen assemblages, together by 1-2% sporinite, 3-15% vitrinite, and 5-10% inertinite for the marl sample ( Table 2). The marls contain more hydrogen-rich AOM (75-90%), with much less inertinite and vitrinite (Table 2), which fit well with characteristics of type I-II 1 kerogen.
The kerogen in mudstones is composed of 50-72% AOM, 1-6% sporinite, 12-22% vitrinite, and 9-31% inertinite. There is no appearance of amorphous humic material, indicating little input of land plants [25]. AOM is associated with import sources of bacterial phytoplankton and algae from surface of lacustrine [26]. Taking into account the geochemical characteristics, it could indicate that OM contribution in the marl comes from more algal or bacterial phytoplanktonic sources, while less bacteria and algae contribution in the mudstone could be confirmed. Vitrinite reflectance is used to determine the indicator of maturity. In the mudstones, only one data was obtained (0.58), but the Ro values of marl are 0.55-0.73.

Biomarkers
5.3.1. Normal Alkanes and Isoprenoids. The gas chromatograms of saturated hydrocarbons separated from Fengcaogou in Wudaoliang Group of WHXB are shown in Figure 5 and results are shown in Table 3. Saturated hydrocarbons of mudstone and marl reveal the dominance of middle to high carbon number molecular; the carbon peak is n-C 23 (e.g., P02-13S3), n-C 27 , n-C 29 (e.g., P02-5S6 and P02-7S1), or n-C 31 (e.g., P02-3S1). The value of C 21− /C 21+ of Fengcaogou mudstones and marls changes from 0.06 to 0.24; all samples show superiority of long-chain n-alkanes, which indicate terrestrial higher plant-derived n-alkanes [27]. The distributions of n-alkanes in the samples have an odd (nC 27,29,31 )over-even (nC 26,28,30 ) carbon number predominance in the nC 23 to nC 31 range ( Figure 5). The OEP vary between 1.45 and 6.91, and most of the samples have the CPI values changing from 4 to 1.75. Long-chain n-alkanes (nC 27 to nC 31 ) are considered coming from terrestrial plant waxes [28]. Thence, predominate of long-chain n-alkanes (e.g., P02-3S1, P02-5S4, P02-5S6, and P02-13S1 besides P02-13S3) can be confused originating from terrestrial plants. But this interpretation is in contradiction with petrographic investigation of kerogens.      6 Geofluids

Geofluids
It has been proved that some nonmarine algae also may be the origin of long-chain n-alkane [29]. Therefore, nonmarine algae and higher plants may be the parent material of longchain odd n-alkanes together. The mid molecular weight of n-alkanes (nC 21 to nC 25 ) is probably considered coming from aquatic macrophytes (predominate of nC 23 and nC 25 ) and Sphagnum [30,31]. And the intermediate molecular weight of n-alkanes found relative contents in most of the samples, especially in P02-7S1. Because the causation of peat bog was precluded, the source of OM from Sphagnum may be excluding and the source of macrophytes leads to the n-alkane patterns. The research shows that the upper strata of Wudaoliang Group (P02) developed a lacustrine sedimentary system. Therefore, n-alkanes of intermediate molecular weight may have originated from macrophytes. By the calculation of P aq = ðC 23 + C 25 Þ/ðC 23 + C 25 + C 29 + C 31 Þ, values of all the samples (averaging 0.42) indicated that the submerged/floating macrophytes were the contributors [30] ( Table 3).
Phytane is the dominant acyclic isoprenoid in the samples of WHXB but has a lower peak than n-alkanes in the samples ( Figure 5). The oxic/anoxic or the origin of OM is judged frequently by the parameter of pristane/phytane (Pr/Ph) ratio [32]. If phytol side chain of chlorophyll from organic matter was oxidized, it would cause priority to form pristine with high Pr/Ph ratios [33]. The values of Pr/Ph of the mudstone and marl samples are relatively low in WHXB changing from 0.11 to 0.36 (average 0.19) ( Table 3). Mudstones from Fengcaogou section exhibit the values of Pr/Ph changing from 0.12 to 0.36. However, Pr/Ph ratios of marl indicate a lower value.
Generally, Pr/Ph > 1 suggests an oxic condition, but Pr/ Ph < 1:0 shows anoxic source-rock deposition [34]. However, several studies indicated that the source input and thermal maturation and other factors can affect the Pr/Ph ratios   9 Geofluids column increasingly and an anoxic condition at the bottom of the lake. The ratios of Ph/n-C 18 and Pr/n-C 17 are shown in Table 3.

5.3.2.
Terpanes. Gammacerane first found in bitumen of the Green River shale are detected in both mudstone and marl samples ( Figure 5) [37]. The ratio of gammacerane/C 31 hopane ((22S+22R)/2) changes from 0.36 to 0.89 in Fengcaogou section. The appearance of gammacerane suggests the hypersaline, reducing sedimentary environment [38,39]. Gammacerane originated from continental and oceanic sedimentary environments with stratified water column [40]. Gammacerane are found in freshwater lacustrine sediments too. In chemocline of stratified water column, there exists tetrahymanol as precursor of gammacerane; tetrahymanol originates from anaerobic ciliates [40]. Because of density-stratified hypersaline water columns, the compounds can get together in the lacustrine environment. The value of Pr/Ph < 0:5 is considered associated with hypersaline environment [41]. The relevance of gammacerane indices and Pr/Ph value in Fengcaogou supports the inferred salinity relationship ( Figure 6). Therefore, Fengcaogou sedimentary rocks might deposit in hypersaline lacustrine condition. The high salinity was accompanied by anoxic condition in bottom water and water column density stratification.
The relative abundances and distribution pattern of pentacyclic and tricyclic terpanes detected by m/z 191 ion chromatograms are listed in Table 2 and Figure 5. Tricyclic terpanes have little content from mudstone and marl and are composed by C 21 -C 24 with the peak at C 23 . In the present studies, it was found that the tricyclic terpanes may originate from some algae or lipids of bacterial membrane [42,43]. And tricyclic terpanes can be used as parameters of depositional environment. Their relatively low concentrations and the low ratios of tricyclic/pentacyclic terpanes (<0. 25) in all samples from the mudstone and marl in WHXB indicate that the biomarkers originate from nonoceanic organism precursor [44,45].
The primary pentacyclic terpanes with the peak at C 30 hopanes are detected from the m/z 191 fragmentograms, and a lot of homohopanes (C 31 -C 35 ) are found in most of the samples ( Figure 5). Ourisson et al. [46] proposed that homohopanes (C 31 -C 35 ) originated from bacteriohopanetetrol and other hopanoids of bacteria in chemocline of stratified water column.

Steranes.
The regular steranes were detected from extracts of mudstone and marl in WHXB showed by m/z 217 mass chromatograms with variable peaks ( Figure 5). Most of the samples from profile indicated a higher ratio of C 27 sterane compared to C 29 sterane or C 28 sterane (6.82%-20.74%), while some samples (P02-5S2, P02-5S4, and P02-5S6) have C 29 > C 27 sterol distribution ( Table 3). The marl is dominated by C 27 sterane (46.6%-48.5%, averaging 47.59%). Volkman [47] and Peters and Moldowan [48] suggest that C 29 sterols originate from land higher plants and C 27 sterols are derived from aquatic algae. Later, Volkman [49] and Volkman et al. [50] suggested that cyanobacteria or microalgae may be the main origin of C 29 sterols too. Here, the predominance of C 29 steroids in mudstones of the middle part in the Fengcaogou section shows a proportion contribution of terrestrial plant; however, C 27 steroids dominant at the lower and upper part of profile may reflect the contribution of algae. With samples from Fengcaogou strata, the explanation of dominant C 29 steroids is inconsistent with maceral composition and other parameters (hopanoids). Phytane can reflect the contribution of archaebacteria and haloalkaliphilic bacteria [49], and thus, massive phytane in the Fengcaogou samples may originate from bacteria and would not rule out higher plants. Hopanes root from hopane polyols, and hopane polyols  10 Geofluids are discovered from cyanobacteria or bacterial membranes [29]. All in all, a large number of phytane suggest the contribution of bacteria or higher plants. Associated with other feature of biomarker and petrographic observation, the evidence indicates that the predominance of C 29 steroids originates from microalgae and bacteria or higher plants. Steranes show the pattern of C 27 > C 28 < C 29 , showing complex origination from algae, bacteria, or wax of terrestrial plant [48].
5.4. Analysis of C Isotopes. Lake sediments can provide the effective ancient environmental information. Because the source of organic matter, paleoclimate, atmospheric CO 2 concentration, and water chemistry of lakes is the influencing factors, the explanation of carbon isotopic ratios is a complex problem [51]. The 13 C value change could be caused by P CO 2 , lake surface variation [52], lake trophic status, biological community, obvious climate changes [19], or the diversification of productivity [19,53]. The mudstones or marls (e.g., P02-13S1) had obviously heavier carbon isotopic composition in kerogen, changing in δ 13 C of considerable OM from −20‰ to −25.8‰ with an average of −23.4‰ (Table 2). In Indonesia, a homologous isotopic feature was found in Pediastrum and Botrycoccus algal shales [54]. Enrichment in 13 C of Cenozoic oil shale was found in Australia too [55]. The enrichment in 13 C of OM from Cretaceous shales has been found in the northern Tibet plateau with a range of −20.79‰ to −21.78‰ [19].
By analyzing the 13 C org in 12 sediment cores from lakes, Stuiver [56] found that the low 13 C org value corresponded to the colder climate during low productivity period and the high 13 C org value corresponded to the warmer climate with higher productivity in the lake. If the organic productivity was increased in lakes, aquatic plants would increase the absorption of 12 CO 2 selectively. Then, this caused the improvement of concentration of 13 C in HCO 3 , resulting in the value increasing of 13 C org of aquatic plant [57]. The closed inland lake in the arid and semiarid area, when the water increased, the biological productivity increased, submerged/floating macrophytes used HCO 3 or dissolved CO 2 as main carbon source, resulting in the increasing of 13 C org ; conversely, when there is drought, the value of 13 C org reduced [58]. Hypersalinity may lead to the heavy isotopic composition in the environment of microbial mats [59], but hypersalinity is not the only causation [19]. High productivity that occurred in microbial/algal mats has been suggested as the cause of abating fractionation of 13 C [60]. Therefore, high productivity leads to the enrichment in 13 C in the lake ecosystem. OM of mudstones and marls in the Fengcaogou section of the WHXB show different 13 C enrichment. The 13 C of marl exhibit the values ranging from −20‰ to −21.9‰, whereas the 13 C of the mudstone samples exhibit a lighter value ranging from −23‰ to −25.8‰. This indicates the raising of productivity.
Moreover, similar source organisms have been confirmed between mudstones and underlying marl, so the OM in samples should show consistent isotopic trends. However, there is virtually no consistent tendency. OM of mudstone P02-9S suggest no enrichment in 13 C relative to marls. Therefore, the enrichment of 13 C cannot be triggered by the source organisms. The exuberant productivity with algae and bacteria is the main factor for the enrichment in 13 C [61-63].

Paleoenvironmental Significances
The evolution of lacustrine paleoenvironment during Oligocene and Miocene of the Hoh Xil basin of has been studied frequently. The lake level fluctuation, lake productivity, geochemical proxies of water, and the feature of organic geochemistry are closely related with tectonic movement and climatic factors [64][65][66][67]. The main reason of the formation of carbonate saline lake is the input of outside material continuously in the humid environment with the tendency of wet conditions [68,69]. In contrast, in the extreme arid climatic conditions, evaporation exceeding precipitation would lead to the concentration of water, with sulfate deposits appearing in saline lake [65]. Major petrological and geochemical factors in sedimentary sequence of Neogene Wudaoliang Group in WHXB suggest the condition of lacustrine water chemistry. Wang [23] reported that Miocene hydrocarbon source rock of Zhuonai Lake in the Hoh Xil basin deposited in a freshwater lake. And paleoclimatic variation from dry to humid caused the transformation of water chemistry, which brought the saline water to fresher water during Oligocene to early Miocene in lakes. There were many tectonic activities, which are accompanied by the uplift of Tibet and paleoclimate and lake ecosystem [70][71][72][73][74][75]. DeCelles et al. [76] suggested that beneficiation of δ 18 O and δ 13 C in carbonates of Nima basin indicated strong evaporation and the arid climate during Oligocene. Wu et al. [77] studied the fossils of vegetation; they suggested that there was a dry, warm climate in Oligocene and a wet, cool climate in early Miocene in central Tibetan Plateau. All evidences suggest that in central Tibet exists the development of saline paleolakes and arid climate in Oligocene. In the early Miocene, many evidences show that the climate of central plateau turns to humid. Accompanied with turning of climate during early Miocene time, two paleolakes covered plateau characterized by the Wudaoliang Group with coniferous trees [77]. Wudaoliang Group greatly distributes in HXB during the early Miocene with freshwater lacustrine limestone, which shows that large paleolake exists, the paleolake named "Wudaoliang paleolake." Miocene lacustrine stromatolites were found in Wudaoliang Group in the Hoh Xil basin, which indicated abnormal humid period [78]. Cai et al. [79] suggest that "Wudaoliang paleolake" turns from a playa lake to the freshwater lakes with the precipitation exceeding evaporation in humid climate. Yi et al. [80] indicated that northern Tibetan Plateau climate evolved to enter a humid stage in the early Miocene and paleolake water salinity obviously dropped and reflected water level rise in lower Wudaoliang Formation by using boron concentrations in lacustrine mudstone. Oxygen and isotopes in the Wudaoliang Group showed a humid condition during the lacustrine sedimentary period from ð24:1 ± 0:6Þ Ma to ð14:5 ± 0:5Þ Ma [81]. The above information and organic geochemical investigation indicated that the lacustrine ecosystem was 11 Geofluids adjusted and updated in the early Miocene characterized by humid condition and productivity improvement.

Conclusions
The lacustrine sediment samples from the Miocene Wudaoliang Formation sections of western Hoh Xil basin in Tibetan are studied in order to appraise biologic-source constitution, sedimentary environment, and maturity of organic matter, reconstruct paleolake environment, and deduce paleoclimatic change information.
(1) Organic matter abundance of samples is low, and average organic carbon content of mudstone and marlite is, respectively, 0.19% and 0.14%. Organic matter of mudstones is mainly types II and III and is in immaturity-low maturity stage, while organic matter of marl is mainly type I-II 1 and is in low maturity-maturity stage (2) The biomarker characteristics indicate that the main sources of the organic matters are algae and bacteria and higher plants. Some of the biomarkers indicate that the sedimentary environment is characterized by the reduced lake conditions and stratified water column (3) The samples from the Fengcaogou section in the WHXB have obviously heavy C isotopic composition. The enrichment in 13 C is caused by elevated productivity (4) The paleoclimate of the western Hoh Xil basin in early Miocene for depositing mudstone and marl became more humid

Data Availability
The data used to support the findings of this study are included within the article.

Conflicts of Interest
The authors declare that they have no conflicts of interest.