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Abstract

A fluid inclusion petrographic and microthermometric study was performed on the sandstones gathered from the Yanchang Formation, Jiyuan area of the Ordos Basin. Four types of fluid inclusions in quartz can be recognized based on the location they entrapped. The petrographic characteristics indicate that fluid inclusions in quartz overgrowth and quartz fissuring-I were trapped earlier than that in quartz fissuring-IIa and fissuring-IIb. The homogenization temperature values of the earlier fluid inclusions aggregate around 80 to 90°C; exclusively, it is slightly higher in Chang 6 member, which approaches 95°C. The later fluid inclusions demonstrate high homogenization temperatures, which range from 100 to 115°C, and the temperatures are slightly higher in Chang 9 member. The calculated salinities show differences between each member, including their regression characteristics with burial depth. Combining with the vitrinite reflection data, the sequence and parameters of fluid inclusions indicate that the thermal history of the Yanchang formation mostly relied on burial. Salinity changes were associated with fluid-rock interaction or fluid interruption. Hydrocarbon contained fluid inclusions imply that hydrocarbon generation and migration occurred in the Early Cretaceous. The occurrence of late fluid inclusions implied that quartz cement is a reservoir porosity-loose factor.

Keywords

Fluid inclusion homogenization temperature salinity quartz precipitation petroleum accumulation Ordos Basin

Introduction

Fluid inclusions are micro-scale samples of fluids, which were trapped during the evolution of sedimentary basins, and can be used to identify the composition of fluids associated with diagenetic and post-diagenetic processes (e.g. Conliffe et al., 2017). Fluid inclusions could be revised depending on the geological events they undergone after entrapment. However, the confined burial processes preferentially keep them original. These undisturbed fluid inclusions held the pore fluid where the inclusions were trapped throughout the geological history steadily. Consequently, the geological information hidden in these undisturbed fluid inclusions can be used to reveal the geothermal and geochemical environments when the entrapment occurring (e.g. Dolníček et al., 2012; Karim et al., 2012; Osborne and Haszeldine, 1993; Parnell et al., 1996; Rossi et al., 2002). Thus, the evolution processes of sedimentary rocks can be re-established by systematical research of fluid inclusions.

Volumetrically, quartz cement is the most important diagenetic phase in buried sandstone (Anovitz et al., 2015; Bjørkum et al., 1998; Robinson and Gluyas, 1992; Taylor et al., 2010). Much effort has been dedicated to understanding the quartz precipitation in burial sandstones (e.g. Hiatt et al., 2007; Marchand et al., 2001; Milliken et al., 2016; Robinson and Gluyas, 1992; Robinson et al., 1992; Worden et al., 1998). Fluid inclusions occur in quartz cement abundantly companied by the diagenetic events of quartz growth or cementation. The investigation of using the high-resolution microscope to determine the sequence of the quartz cementation can clarify the sequence of the fluid inclusion simultaneously. These substantially support the researches of geothermal and geochemical environments evolution and quartz precipitation in burial sandstone.

The Ordos Basin has undergone continuous depression in Triassic as an inland lake before it starts uplifting at the end of the Early Cretaceous (Ren et al., 2007). The stable sedimentation accretes thick clastic rocks, the Yanchang Formation, which has been subdivided into ten members (Chang 10 to 1 from bottom upward). The basin evolution and its thermal history has been addressed by modeling (e.g. Chen et al., 2006; Kuang et al., 2004; Ren, 1996; Ren et al., 1994, 2007, 2017; Ren and Zhao, 1997), which shows the general burial history of the Ordos Basin. The Chang 7 member, which has abundant lacustrine mudstones, dominated the petroleum sources with high quality of hydrocarbon generation (e.g. Xi et al., 2008; Yang et al., 2013, 2016; Yang and Zhang, 2005; Zhang et al., 2006). The Chang 6 member above, and the Chang 8, 9 members blow it are the main reservoirs in the Yanchang Formation, which generally presenting low porosity and permeability (e.g. Lan et al., 2014; Li et al., 2016; Zhou et al., 2016; Zhu et al., 2015). The reservoir qualities have been addressed by many researchers and concluded that it’s dominated by compaction and cementation (e.g. Luo et al., 2006; Zhang et al., 2017; Zhou et al., 2016). However, the coupling evolution of the thermal environment, reservoir quality, and hydrocarbon accumulation is still unclear. This paper addressed four members (from Chang 9 to 6) in the Jiyuan area to investigate the hydrothermal environment that these formations have undergone and to reveal the diagenetic events and hydrocarbon recourses using fluid inclusion and vitrinite reflectance data.

Geological setting

The Ordos Basin is located in northern China and covers an area of approximately 37 × 10⁴ km² (Figure 1(a)). It ranks the second largest sedimentary basin in size and has the highest hydrocarbon potential in China (Dai et al., 2016). Above the Archean and Proterozoic crystalline basement rocks, deposited a series of sedimentary rocks (Dai et al., 2016; Wang, Sandvol, et al., 2014). In the early Paleozoic, the Ordos Basin was covered by shallow marine, and carbonate developed immensely in the tectonic environment of the Craton margin. This situation was transformed by the later Paleozoic, which before the basin undergone depression as an inland basin. Indonesian movement at the end of the Paleozoic entered the basin into the inland rifting and subsiding period (Chen et al., 2006). The orogeny in the west and south of the basin led to rapid subsidence in the southwest, initiating from the beginning of the Mesozoic. The orogeny shaped the morphology of the basin higher in the northeast and lower in south and west, which determined steady deposition in the southwest (from Guyuan to Huanxian) of the basin in the Triassic (Wang, 2017; Yang, 2002) (Figure 1(a)), and the Yanchang Formation was developed in the Late Triassic.

Figure 1.

(a) The schematic diagram of the tectonic setting of the Ordos Basin and the location of the research area. (b) A diagram of stratigraphy, sedimentary log, sedimentary environment interpretation, and lake level changes of the Yanchang Formation.

Slightly uplift occurred at the end of the Triassic, driven by the Yanshan movement. The uplift caused erosion, which wiped Chang 1, Chang 2, and partial Chang 3 members in the southwest of the basin. However, the uplift didn’t change the tectonic regime generally, the subsidence and deposition occurred subsequently. Cyclic tectonic movement uplifted the basin several times in the Jurassic, which led to erosion and unconformable depositions, but the general subsidence brought the strata going deeper until the end of early Jurassic, then the last stage of the Yanshan movement uplifted the basin gradually (Chen et al., 2006; Ren et al., 2007; Yang, 2002). During the Cenozoic, several grabens developed around the Ordos basin (Ritts et al., 2009; Wang, Sandvol, et al., 2014). In present, the basin can be divided into six tectonic units: the Yimeng Uplift, Western Thrust Belt, Tianhuan Sag, Yishan Slope, Jinxi Flexure Belt, and the Weibei Uplift (Figure 1(a)). The study area is located in the southwest part of the basin across the Tianhuan Sag and Yishan Slope (Figure 1(a)). Faults and folds restrained the margins of the basin, and the principal part of the basin dips to the west gently (e.g. Zou et al., 2012).

The evolution of the Ordos Basin during the Paleozoic-Mesozoic is divided into three stages (Yang et al., 2005). (1) From Cambrian to Early Ordovician, the basin was occupied by shallow-marine and tidal-flat as a part of the craton basin margin; (2) From Middle Ordovician to Middle Triassic, it was surrounded by convergent margins, and the south of the basin was mainly dominated by thinly bedded marine sediments; and (3) From Late Triassic to Early Cretaceous, it transformed into a complete intraplate basin by the collision and convergence between the North and South China blocks, the Qiangtang block, and the Eurasian plate. The basin underwent a transition from an open marine environment to a non-marine lacustrine environment (Yang et al., 2005; Zou et al., 2012).

The Yanchang Formation, which developed in the Upper Triassic, was subdivided into ten members (Chang 10 to Chang 1 from bottom upward), and experienced a complete cycle of lake development: the initial formation and development stage (Chang 10 to Chang 8); peaking stage (Chang 7 to Chang 4 + 5) and declining stage (Chang 3 to Chang 1) (Xu et al., 2016; Zou et al., 2008). The maximum water level was reached during Chang 7 period, and the deepest part of the lake was located in the southwest and partly northeast (Xu et al., 2016). Siliciclastic sediments composed the Yanchang Formation, including fluvial, delta, debris, lacustrine sediments and others (Figure 1(b)), which accreted for more than 3,000 m (approximately 10,000 ft) in the southwest and about 1,000 m (approximately 3,200 ft) in the east of the Ordos Basin (Zhou et al., 2016). Shallow-lacustrine sand-rich deltas and associated fluvial developed extensively and form the main reservoir rocks in The Yanchang Formation (Zou et al., 2010, 2012). Chang 9 and Chang 8 members were dominated by fluvial sediments in the study area, which consisted of coarse to medium sand with abundant sedimentary structures (Figure 1(b)). Chang 7 member developed when the lake level abruptly rise (Figure 1(b)). Lacustrine mud and fine-grained delta sediments are predominated in this semi-deep and deep lake settings, forming high-quality hydrocarbon source rocks with an average TOC of 13.75% and a vitrinite reflectance (Ro) in the range of 0.85% - 1.15% (Xi et al., 2008; Yang and Zhang, 2005; Zhou et al., 2016). Regression of the lake started from Chang 6 member, and it was filled by delta and fluvial sediments. Chang 9, Chang 8, and Chang 6 are the main reservoirs in the Yanchang Formation (Figure 1(b)).

Samples and methods

The samples for analysis of fluid inclusions were collected from core intervals from 17 wells. There are seven samples from Chang 6 member, eight samples from Chang 7 member, six samples from Chang 8 member, and one sample from Chang 9 member. The fluid inclusions are hosted in quartz. Cold techniques and ultraviolet-light-sensitive epoxy, which can avoid thermal re-equilibration of fluid inclusion, were used for doubly polished thick sections during the sample preparation.

The measurement of the homogenization temperature of the inclusions follows the general method that O’Reilly et al. (1998) and Zhao et al. (2002) documented. The fluid inclusions first were fund and marked on the thick sections by optical microscope, and then the marked samples will be transported to the microscope equipped with a heating-freezing stage. The petrography of the fluid inclusions, including the shape, size, color, phase, location, sequence, and quality, was identified by using high magnification (200 to 400 magnification). And then the homogenization temperatures were determined by heating the fluid inclusion 5°C/min. The salinity of the inclusions was calculated from ice melting temperature according to the equation of Bodnar (1993). Several fluid inclusions failed to re-nucleate a vapor bubble after heating to the homogenization temperature. This situation even continued after prolonged cooling or standing at room temperature for a long time.

Followed the documentation of Schito et al. (2016), mean random vitrinite reflectance (R_o %) was measured on concentrated organic matter prepared using the traditional HF-HCl method (Robl and Davis, 1993). Samples were first mounted in epoxy resin and polished. Vitrinite reflectance analyses were then performed on randomly oriented grains.

Results

Fluid inclusion petrography

Fluid inclusions could be subdivided into four types based on the location that they were entrapped in the quartz and the sequence that they were entrapped. Two periods of quartz cementation were recognized. In the earlier quartz cementation, the fluid inclusion is developed with (i) quartz overgrowth (Figure 2) and (ii) quartz fissuring (quartz fissuring-I) (Figure 3); and in the later quartz cementation, the fluid inclusions are associated with the fissuring mainly, including that (iii) developed inside of quartz (quartz fissuring-IIa) (Figure 4(a) and (b)), and (iv) traversed the whole quartz grains including the overgrowth part (quartz fissuring-IIb) (Figure 4(c) and (d)). The sequence of the quartz cementation is identified by the spatial relationship between overgrowth quartz and fissuring themselves.

Figure 2.

Microphotographs of fluid inclusions entrapped by quartz overgrowth. (a) and (b) Quartz overgrowth (Qtz-og) trapped fluid inclusions that lined along the edge of detrital quartz (DQ); (c) and (d) Hydrocarbon contained fluid inclusions (red arrows pointed) in the quartz overgrowth are illustrated by fluorescence technique.

Figure 3.

Microphotographs of earlier fluid inclusions entrapped in quartz fissuring (quartz fissuring-I). (a) and (b) The fissuring occurred inside of the detrital quartz (DQ) trapped fluid inclusions. Some primary inclusions were derived from the origin of detrital quartz. The organically enriched matrix filled up the intergranular space of detrital quartz and plagioclase (Pl). (c) and (d) The hydrocarbon contained fluid inclusions (red arrows pointed) sporadically arrayed in the micro-fissuring of detrital quartz (DQ), and show light blue in fluorescence. The little bobs suggest slightly gas including.

Figure 4.

Microphotographs of later fluid inclusions entrapped in quartz fissuring. (a) and (b) Conjugated fissuring inside of the detrital quartz grain (DQ) trapped fluid inclusions (quartz fissuring-IIa), and the fissuring subparallel occurred in the adjacent quartz grains. Organic enriched matrix and calcite cement (Ca) fill in the intergranular pores. (c) and (d) Conjugated fissuring traverse the detrital quartz grain (DQ), and trapped hydrocarbon contained fluid inclusions serially (red arrows pointed, quartz-fissuring-IIb).

Quartz overgrowth in Yanchang sandstone was recognized growing in the eodiagenesis stage. The fluid inclusions entrapped in these quartzes are the earlier ones (Figure 2). Concurrently, the early physical mechanism ruptured while the quartz grains occurred, which entrapped fluid inclusions as earlier ones (Figure 3). These two kinds of earlier fluid inclusions may have different formation times, but hard to be investigated by microscope precisely. Generally, they occurred in the eodiagenesis stage when the temperature is low. The later fluid inclusions were mainly entrapped in the fissuring of quartz, both inside fissuring and traverse fissuring (Figure 4). The late fissuring usually conjugated occurred due to tectonic stress (Figure 4). The crosscutting relationship makes the inside fissuring easily to be distinguished from the earlier fissuring. And the traversing fissuring, particularly the ones that cross the overgrowth quartz, constrained these fluid inclusions to occur later. Commensurately, the relative formation time of these two types of later fluid inclusions is hard to be determined accurately, but they all presented later than the quartz overgrowth and quartz fissuring-I types.

The fluid inclusions are regular in morphology, spreading along the rim of the overgrowth or fissuring. The size of the inclusion is small; the diameters are around several millimeters. The color of the fluid inclusions appears to be dark brown, light yellow, or gray under the microscope. The composition is dominated by liquid water containing hydrocarbon (Figures 2(d), 3(d), and 4(d)). Some of them contain gas slightly (<5%) (Figure 3(c)).

Microthermometry and salinity

In the Chang 6 member, the homogenization temperature value of the earlier fluid inclusions range from 81 to 104°C (about 90°C on average, n = 11) (Figure 5(a), Table 1), most of them are in inside fissuring; their salinity value (eq. NaCl) range from 0.35 to 3.71 wt. % (about 1.61 wt. % on average, n = 11) (Figure 5(b), Table 1). And the homogenization temperature value of later fluid inclusions ranges from 77 to 103°C (about 103°C on average, n = 31) (Figure 5(a), Table 1); their salinity value ranges from 1.06 to 11.61 wt. % (about 5.80 wt. % on average) (Figure 5(b), Table 1). Generally, the homogenization temperature and salinity of the earlier fluid inclusions are relatively lower than the later ones.

Figure 5.

Histograms illustrate the statistic distributions of the homogenization temperature and salinity value in Chang 6 to 9 members. (a), (c), (e) and (g) Statistic result of the homogenization temperature value of the fluid inclusions in quartz in Chang 6 to Chang 9 members. (b), (d), (f) and (h) Statistic result of the salinity of the fluid inclusions in quartz in Chang 6 to Chang 9 members.

Table 1.

The homogenization temperature and salinity data of the fluid inclusions from the Chang 6 to Chang 9 members in the Jiyuan area, Ordos Basin.

Member ID	Sample ID	Depth (m)	Homogenization temperature (^oC)	Salinity (wt.% NaCl eq.)	Sequence of the fluid inclusions
Chang 6	B32-c6-1	2409.50	95	2.41	O1
	B32-c6-2	2409.50	93	1.91	F1
	B32-c6-3	2409.50	90	1.74	F1
	B32-c6-4	2409.50	104	0.53	F1
	B32-c6-5	2409.50	96	0.71	F1
	B138-c6-1	2121.89	88	2.90	F1
	B138-c6-2	2121.89	87	0.53	F1
	B138-c6-3	2121.89	89	1.23	F1
	B138-c6-4	2121.89	87	3.71	F1
	T17-c6-1	1425.50	81	0.35	F1
	T17-c6-2	1425.50	83	1.74	F1
	B284-c6-1	1734.55	112	4.80	F2a
	B284-c6-2	1734.55	83	8.81	F2a
	B284-c6-3	1734.55	77	2.74	F2a
	B284-c6-4	1734.55	79	3.06	F2a
	S103-c6-1	2033.68	106	5.41	F2a
	T17-c6-3	1425.50	95	1.06	F2a
	W56-c6-1	2016.30	103	3.39	F2a
	W56-c6-2	2016.30	113	2.07	F2a
	W56-c6-3	2016.30	109	5.71	F2a
	W56-c6-4	2016.30	89	3.87	F2a
	W56-c6-5	2016.30	96	3.87	F2a
	W56-c6-6	2016.30	87	4.34	F2a
	W56-c6-7	2016.30	93	3.87	F2a
	W56-c6-8	2016.30	89	3.71	F2a
	W62-c6-1	1796.50	103	10.49	F2a
	W62-c6-2	1796.50	104	10.61	F2a
	W62-c6-3	1796.50	103	10.73	F2a
	W62-c6-4	1796.50	126	3.71	F2a
	W62-c6-5	1796.50	112	2.74	F2a
	W62-c6-6	1796.50	119	6.74	F2a
	W62-c6-7	1796.50	116	6.45	F2a
	B284-c6-5	1734.55	102	2.57	F2b
	B284-c6-6	1734.55	108	2.41	F2b
	B284-c6-7	1734.55	100	2.24	F2b
	B284-c6-8	1734.55	103	2.07	F2b
	B284-c6-9	1734.55	101	11.61	F2b
	B284-c6-10	1734.55	121	11.33	F2b
	B284-c6-11	1734.55	120	11.47	F2b
	B284-c6-12	1734.55	110	11.19	F2b
	B284-c6-13	1734.55	105	11.05	F2b
	S103-c6-2	2033.68	103	–	F2b
Chang 7	B32-c7-1	2454.50	78	1.23	O1
Chang 7	B32-c7-2	2454.50	80	1.05	O1
	B32-c7-3	2454.50	90	2.90	O1
	B32-c7-4	2454.50	105	4.18	O1
	B32-c7-5	2454.50	95	5.71	O1
	B32-c7-6	2454.50	97	6.59	O1
	B32-c7-7	2454.50	99	5.86	O1
	B244-c7-1	2118.40	99	2.74	F1
	L122-c7-1	2360.00	95	3.06	F1
	L122-c7-2	2360.00	97	3.39	F1
	L122-c7-3	2360.00	89	4.34	F1
	L122-c7-4	2360.00	89	5.41	F1
	N44-c7-1	1514.30	89	1.74	F1
	N44-c7-2	1514.30	83	9.47	F1
	N44-c7-3	1514.30	93	1.40	F1
	X63-c7-1	1816.43	87	1.74	F1
	X63-c7-2	1816.43	97	9.98	F1
	Z33-c7-1	1713.10	80	14.77	F1
	Z33-c7-2	1713.10	72	3.87	F1
	Z33-c7-3	1713.10	73	3.87	F1
	Z33-c7-4	1713.10	74	3.71	F1
	Z33-c7-5	1713.10	70	4.18	F1
	Z33-c7-6	1713.10	74	3.39	F1
	Z59-c7-1	1565.30	85	4.65	F1
	L122-c7-5	2360.00	83	1.06	F2a
	L122-c7-6	2360.00	106	10.49	F2a
	L122-c7-7	2360.00	107	10.73	F2a
	L122-c7-8	2360.00	113	7.31	F2a
	L122-c7-9	2360.00	103	5.41	F2a
	N44-c7-4	1514.30	106	2.75	F2a
	N44-c7-5	1514.30	110	2.24	F2a
	W56-c7-1	2054.16	114	5.41	F2a
	W56-c7-2	2054.16	113	5.41	F2a
	W56-c7-3	2054.16	112	5.26	F2a
	W56-c7-4	2054.16	103	5.41	F2a
	W56-c7-5	2054.16	110	5.56	F2a
	W56-c7-6	2054.16	93	0.88	F2a
	W56-c7-7	2054.16	119	5.26	F2a
	W56-c7-8	2054.16	90	1.40	F2a
	W56-c7-9	2054.16	95	1.57	F2a
	W56-c7-10	2054.16	108	2.07	F2a
	W56-c7-11	2054.16	125	1.74	F2a
	W56-c7-12	2054.16	115	8.81	F2a
	W56-c7-13	2054.16	100	1.91	F2a
	X63-c7-3	1816.43	111	3.06	F2a
	X63-c7-4	1816.43	113	2.57	F2a
	Z33-c7-7	1713.10	83	6.88	F2a
	Z59-c7-2	1565.30	81	6.45	F2a
	Z59-c7-3	1565.30	109	3.39	F2a
	Z59-c7-4	1565.30	111	3.23	F2a
	Z59-c7-5	1565.30	110	3.06	F2a
	Z59-c7-6	1565.30	111	2.41	F2a
	Z59-c7-7	1565.30	112	6.16	F2a
	Z59-c7-8	1565.30	106	6.01	F2a
	Z59-c7-9	1565.30	110	5.86	F2a
	B244-c7-2	2118.40	115	2.57	F2b
	B244-c7-3	2118.40	111	1.40	F2b
	B244-c7-4	2118.40	113	1.23	F2b
	B244-c7-5	2118.40	122	10.98	F2b
	L122-c7-10	2360.00	71	7.73	F2b
	N44-c7-6	1514.30	105	2.07	F2b
	N44-c7-7	1514.30	110	1.74	F2b
	X63-c7-5	1816.43	115	5.86	F2b
	X63-c7-6	1816.43	117	5.56	F2b
Chang 8	Y177-c8-1	2468.10	81	1.57	O1
	Y177-c8-2	2468.10	80	1.40	O1
	B244-c8-1	2245.40	89	4.80	F1
	B244-c8-2	2245.40	93	3.55	F1
	B244-c8-3	2245.40	95	3.55	F1
	B244-c8-4	2245.40	93	4.96	F1
	B244-c8-5	2245.40	84	16.05	F1
	B284-c8-1	1857.90	74	8.68	F1
	B284-c8-2	1857.90	72	9.21	F1
	L79-c8-1	2338.38	96	4.03	F1
	L79-c8-2	2338.38	93	3.71	F1
	Y177-c8-3	2468.10	83	1.23	F1
	Y177-c8-4	2468.10	78	1.06	F1
	Y177-c8-5	2468.10	87	1.06	F1
	Y177-c8-6	2468.10	83	1.40	F1
	Y177-c8-7	2468.10	79	2.24	F1
	Y177-c8-8	2468.10	83	2.24	F1
	Y177-c8-9	2468.10	84	1.06	F1
	Y177-c8-10	2468.10	82	0.71	F1
	Y177-c8-11	2468.10	83	0.53	F1
	Y177-c8-12	2468.10	81	0.53	F1
	Y177-c8-13	2468.10	81	0.71	F1
	Y177-c8-14	2468.10	83	0.88	F1
	Y177-c8-15	2468.10	80	0.53	F1
	B244-c8-6	2245.40	120	5.86	F2a
	B244-c8-7	2245.40	120	1.57	F2a
	B284-c8-3	1857.90	116	3.71	F2a
	L79-c8-3	2338.38	85	1.74	F2a
	L79-c8-4	2338.38	120	1.40	F2a
	ZH217-c8-1	2295.54	97	3.71	F2a
	Z59-c8-1	1709.10	112	2.24	F2a
	Z59-c8-2	1709.10	104	2.41	F2a
	Z59-c8-3	1709.10	102	2.74	F2a
	Z59-c8-4	1709.10	102	2.24	F2a
	Z59-c8-5	1709.10	101	1.06	F2a
	B244-c8-8	2245.40	86	3.87	F2b
	B244-c8-9	2245.40	89	3.23	F2b
	B244-c8-10	2245.40	93	4.96	F2b
	B244-c8-11	2245.40	92	4.80	F2b
	B244-c8-12	2245.40	79	5.41	F2b
	L79-c8-5	2338.38	91	2.74	F2b
	L79-c8-6	2338.38	80	2.07	F2b
	L79-c8-7	2338.38	78	1.74	F2b
	L79-c8-8	2338.38	79	1.91	F2b
	Y177-c8-16	2468.10	84	1.74	F2b
	Y177-c8-17	2468.10	89	4.18	F2b
	ZH217-c8-2	2295.54	77	4.34	F2b
	ZH217-c8-3	2295.54	96	1.40	F2b
	ZH217-c8-4	2295.54	75	4.65	F2b
	ZH217-c8-5	2295.54	73	4.34	F2b
	ZH217-c8-6	2295.54	94	1.06	F2b
Chang 9	M23-c9-1	2506.28	101	1.40	F1
	M23-c9-2	2506.28	89	6.30	F1
	M23-c9-3	2506.28	87	3.87	F1
	M23-c9-4	2506.28	77	0.53	F1
	M23-c9-5	2506.28	76	3.87	F1
	M23-c9-6	2506.28	73	1.74	F1
	M23-c9-7	2506.28	113	18.72	F2a
	M23-c9-8	2506.28	116	17.34	F2a

O1: quartz overgrowth; F1: quartz fissuring-I; F2a: quartz fissuring-IIa; F2b: quartz fissuring-IIb

In the Chang 7 member, the homogenization temperature value of the earlier fluid inclusions ranges from 70 to 105°C (about 87°C on average, n = 24) (Figure 5(c), Table 1); their salinity value ranges from 1.05 to 14.77 wt. % (about 4.55 wt. % on average, n = 24) (Figure 5(d), Table 1). The homogenization temperature value of later fluid inclusions ranges from 71 to 125°C (about 104°C on average, n = 40) (Figure 5(c), Table 1), and their salinity value range from 0.88 to 10.98 wt. % (about 4.47 wt. % on average, n = 40) (Figure 5(d), Table 1). The diversity of homogenization temperature values between the earlier fluid inclusions and later ones is distinctive; however, the salinity value doesn’t show obvious diversity in distribution.

In the Chang 8 member, the homogenization temperature value of the earlier fluid inclusions ranges from 72 to 96°C (about 84°C on average, n = 24) (Figure 5(e), Table 1); their salinity value ranges from 0.53 to 16.05 wt. % (about 3.15 wt. % on average, n = 24) (Figure 5(f), Table 1). The homogenization temperature value of later fluid inclusions ranges from 73 to 120°C (about 94°C on average, n = 27) (Figure 5(e), Table 1), and their salinity value is relatively very low, ranging from 1.06 to 5.86 wt. % (about 3.00 wt. % on average, n = 27) (Figure 5(f), Table 1). The difference of the salinity value between the fluid inclusions entrapped in the earlier and later is slight, several high salinity values present in the earlier fluid inclusion.

The samples from the Chang 9 member are limited, only eight fluid inclusions were tested in this study, and six of them are earlier ones. Their homogenization temperature and salinity values vary between 73 to 101°C (about 84°C on average) and 0.53 to 6.3 wt. % (about 2.95 wt. % on average) respectively (Figure 5(g) and (h), Table 1). The two later fluid inclusion samples show relatively high homogenization temperature (114.5°C on average) and salinity (18.03 wt. % on average) (Figure 5(g) and (h), Table 1).

Vitrinite reflectance

The vitrinite reflectance value of the mudstone ranges between 0.64% and 1.09% (0.85% on average). The burial depth of the samples varies from about 1500 to 2430 m (Figure 6, Table 2).

Figure 6.

The plot of vitrinite reflectance (R_o) versus burial depth shows that the R_o rise steadily with the burial depth increasing in the Yanchang Formation.

Table 2.

The vitrinite reflectance data of the samples from the Chang 6 to Chang 9 members in the Jiyuan area, Ordos Basin.

Samples	Member name	Depth (m)	Vitrinite reflectance (R_o %)
Z-1-42	Chang 6	1728.53	0.84
L-1-54	Chang 6	1939.60	0.73
L-1-55	Chang 6	2252.90	0.76
ZH-1-58	Chang 6	2276.50	0.78
Z-1-31	Chang 6	1497.83	0.68
Z-2-31	Chang 6	1498.62	0.72
Z-3-31	Chang 6	1499.33	0.64
L-1-51	Chang 6	2097.20	0.89
ZH-1-43	Chang 6	2175.30	0.95
L-1-52	Chang 6	2187.20	0.84
ZH-2-58	Chang 6	2285.60	0.81
Z-1-19	Chang 6	1947.00	0.78
Z-2-19	Chang 6	1956.70	0.89
L-2-54	Chang 6	1998.40	0.76
ZH-2-43	Chang 6	2215.60	0.99
ZH-1-53	Chang 7	2096.30	0.91
L-2-55	Chang 7	2352.00	0.82
Z-3-19	Chang 7	2015.60	0.87
ZH-1-33	Chang 7	2213.60	0.98
ZH-2-33	Chang 7	2219.40	0.98
L-1-57	Chang 7	2319.25	0.85
Z-1-50	Chang 7	1943.00	0.68
Z-2-50	Chang 7	1943.00	0.68
Z-3-50	Chang 7	1943.20	0.75
Z-4-50	Chang 7	1943.70	0.76
Z-1-66	Chang 7	2048.76	0.87
ZH-1-42	Chang 7	2188.70	1.00
ZH-1-37	Chang 7	2238.20	1.09
ZH-2-37	Chang 7	2239.20	1.02
ZH-3-37	Chang 7	2242.90	1.03
L-2-51	Chang 7	2267.30	0.77
ZH-1-39	Chang 7	2286.06	0.84
ZH-2-39	Chang 7	2287.50	0.90
L-2-57	Chang 7	2333.45	0.88
L-3-57	Chang 7	2338.65	0.88
L-4-57	Chang 7	2346.00	0.84
ZH-3-58	Chang 7	2422.80	0.91

Discussion

Geothermal history and fluid flow

Data obtained from the primary fluid inclusions in quartz cement that grew at different stages during diagenesis provides information about the thermal and compositional evolution of the pore fluids, which can be used to constrain the conditions of the cement formation (Karim et al., 2012). However, Fluid inclusions experienced several detail-unknown geological events after entrapped. The changes in the physical environment (i.e. temperature and pressure) can lead re-equilibrium of the fluid inclusions (Osborne and Haszeldine, 1993, 1995). And thus, the homogenization temperature of the fluid inclusions cannot accurately identify which geological event they subjected to. However, the re-equilibrium of the fluid inclusion requests rigid conditions, and this occurred in the burial history difficultly (Robinson et al., 1992; Sterner and Bodnar, 1989). Furthermore, the burial depth of The Yanchang Formation in the research area is from about 1400 to 2500 m, which argues against the likely burial depth that led to the re-equilibrium of fluid inclusion preferentially. And in the data preparation processes, the performance of stretching or leakage of the fluid inclusions were excluded in the database. However, there still has some unavoidable deviation in the data compiling processes, including the risk in recognition and distinguishing the sequence and generation of the fluid inclusions. But the result of the homogenization temperature data was based on statistical analysis, which shows the general temperature that the quartz growth (Walderhaug, 1994).

The formation of fluid inclusions in quartz cement is favored by saline fluids, which preferentially “wet” the quartz surface by higher temperatures, that result in faster growth of quartz overgrowths (Brantley and Voigt, 1989; Lander et al., 2008; Taylor et al., 2010). Therefore, it is unlikely that the fluid inclusions record the full range of conditions under which quartz cement grew; rather, they preferentially formed at times of higher temperatures (Karim et al., 2012). Besides, rapid burial history after the deposition of the Yanchang Formation elevated the temperature expeditiously (Chen et al., 2006; Kuang et al., 2004; Ren, 1996; Ren et al., 1994, 2007; Ren and Zhao, 1997). This narrowed the range of trapping temperature down, and thus, we postulate the homogenization temperature present the formation temperature when the fluid inclusions were entrapped.

Volcanic activity was frequently assaulted when the Yanchang Formation was depositing (Qiu et al., 2010; Wang, Xin, et al., 2014), and therefore lead to an abundance of hydrothermal sedimentation (He et al., 2016). The entrapment sequence of the fluid inclusions indicates that obvious thermal events absent in the burial processes of the Yanchang Formation. The homogenization temperature varies mainly between 80 to 90°C in the earlier fluid inclusions; and 100 to 115°C in the later fluid inclusions (Figure 5(a), (c), and (e)). Comparing to the burial history, these fluid inclusions are trapped before the tectonic reverse and uplifting initiating, and the depth range from 1800 to 2600 m roughly (Figure 7). Quartz cementation in Chang 6 occurred relative later after deep buried, and preferred when the temperature over 90°C; Chang 8 quartz cement grew earlier, slightly over 80°C. The later fluid inclusions occurred in Chang 9 member at a relatively high temperature than that of other members (Figure 7). This suggests that the depth of quartz cementation varies between different members, which indicated that thermal histories between the members were slightly different. However, the general temperature evolution with the burial processes suggests that thermal events were insignificant in the Yanchang Formation, although there has some report shows mineralogical evidence (Li et al., 2012).

Figure 7.

Schematic burial history curves in Shancan 1 well in the northeast of the research area (modified after Ren et al., 2007) showing a preferred interpretation of entrapment temperatures of fluid inclusions. Dashed lines show isotherms, and black arrow show inferred burial history of sandstones with quartz cement; mean salinity is grayscale coded.

The salinity of the fluid inclusion can reveal the origin and migration scenarios of pore waters. The fluids represent pore waters that were formed by long-term water-rock interactions involving initially low salinity fluids (Karim et al., 2012). It is obvious that the fluids in the inclusions did not result from the simple entrapment of lakewater. Burial processes probably increased the salinity of the pore water, the evidence exists in Chang 6 member, where the salinity increase from 1.5 to 7.3 wt. % NaCl from the earlier fluid inclusion (quartz overgrowth-I) to the later ones (quartz fissuring-IIb) (Figure 5(b)). Chang 7 and Chang 8 fluid inclusions show low-salinity (< 5 wt. % NaCl) in both stages (Figure 5(d) and (f)). The modification of primary low-salinity pore fluids by dehydration reactions involving the formation of clays or other hydrooxysilicates may occur, and the possibility of fluid input must also be considered. It is possible that the high-salinity fluid inclusions in Chang 9 member (17 wt. % NaCl on average in later inclusions) (Figure 6) obtained their dissolved salt from the dissolution of other minerals, these processes may relate to the relatively high temperature they formed and thermal processes the rocks have undergone.

Quartz precipitation

The trapped fluid compositions, trapping pressures, and temperatures affect the variations in homogenization temperature individually or as a combination. The compressibility and the likely uniform sedimentary source constrained the homogenization temperature to the condition of formation temperature. Based on the assumption above, the homogenization temperature closely represents trapping temperature. The precipitation of quartz could be revealed by the fluid inclusions entrapped inside. Further, we assumed that the variance of a sample of homogenization temperatures is numerically approximately equal to the variance of trapping temperatures. The range of trapping temperature is approximately equal to that of the corresponding homogenization temperature, even though the absolute value may be different slightly.

The measured homogenization temperature, therefore, reflects the temperature of quartz cementation approximately. According to the burial history, the range of homogenization temperatures of the fluid inclusions suggests that the quartz growth in the Yanchang Formation continued for a long period. The initial quartz cement occurred as very small overgrowths, probably hard to trap fluid inclusions (Burley et al., 1989). Therefore, the quartz precipitation at least initiated before the earlier fluid inclusion occurred, where the depth is about 1700 m at 190 Ma ago (Figure 7). The burial processes continued to the depth of about 2100 and 2500 m, where the late fluid inclusions were trapped in the fissuring of the quartz (Figure 4), this indicates that the quartz precipitation lasted to 130 Ma ago, when the formation approached the deepest burial (Figure 7). Further, we can infer that the quartz precipitation continued when the basin uplifting as the condition of temperature is enough for quartz growth, of cause, it is also controlled by other factors. It should be pointed out that the trapping temperature is higher than the homogenization temperature. Therefore, the range of duration and depth of quartz cementation diverge slightly.

Stoichiometrically, the precipitation and dissolution of quartz have been researched for a long time (e.g. Carr and Tester, 2013; Dove, 1994; Dove and Elston, 1992; Ganor et al., 2005; Kumar and Ghassemi, 2005; Rimstidt, 1997; Rimstidt and Barnes, 1980; Steele-MacInnis et al., 2012; Williams et al., 2015). Scholars were trying to build a model to explain the chemical equilibrium of dissolution and precipitation of quartz under different solution environment (Carr and Tester, 2013; Ganor et al., 2005; Rimstidt, 1997). The temperature is one of the key factors that can control the rate of quartz precipitation and dissolution. The higher temperature will increase the chemical kinetics of quartz dissolution; however, the concentration of SiO⁴⁻ iron has an opposite function (Dove, 1994; Ganor et al., 2005). The pH of the pore fluid may be decreased by the hydrocarbon generated in Chang 7 Member and migrated into the adjacent members (Chen et al., 2017; Cui et al., 2019; He et al., 2019), which may have a potential advantage for quartz precipitation rather than dissolution. The rate of the quartz precipitation kept in a relatively low magnitude since a high rate of production can create amorphous silica (Ganor et al., 2005; Rimstidt and Barnes, 1980).

Petroleum implication

Chang 7 member is the main source rocks in the Yanchang Formation. Chang 6, Chang 8, and Chang 9 members are the main reservoirs (Li et al., 2011). Deep burial processes matured the source rocks and drove the R_o to a hydrocarbon-potential range (Figure 6, Table 2). The continuous burial propelled the stratigraphy level down and raised the temperature, which is sufficiently prolonged to be expected to have an impact on thermal maturation. After the Cretaceous, the cooling of the basin gradually occurred with the uplift, while R_o stopped rising (Ren et al., 2007). The hydrocarbon fluid inclusions record the time of hydrocarbon generation. The results suggest that the hydrocarbon generation at least started at the end of Jurassic, and sustained to the end of Cretaceous, when the source rocks matured sufficiently involving the value of R_o.

Hydrocarbon fluid inclusions constrain the time of hydrocarbon generation and demonstrate the migration pathways of hydrocarbons in the reservoir rocks by their location (Baron et al., 2008; Conliffe et al., 2017). Growth faulting was active in the southwest Ordos Basin since the Late Jurassic (Chen et al., 2006). The migration of hydrocarbons mainly through the faults from Chang 7 member (source rocks) to the other members (reservoir rocks) (Lan et al., 2014; Xi et al., 2008; Yang et al., 2005, 2013; Zhang et al., 2006). However, the fluid inclusions grew before the faults restrained the time of the hydrocarbon generation and migration, both in the source and reservoir rocks (Figures 2(d), 3(d), and 4(d)). This presumably suggests that the migration of hydrocarbon has initiated before the faults developed in the later Jurassic when the source rocks matured.

The rapid burial destroys the original porosity of the reservoir substantially. The diagenesis processes are the main factors modifying the reservoir quality after deposition (Dutton and Loucks, 2010; Estupinan et al., 2007; Kantorowicz et al., 1987; Zhang et al., 2017). Quartz cementation is one of the porosity-loss factors. However, the quartz precipitation after hydrocarbon emplacement is still under debate. Some researches argue that quartz is water wet and there is always water present in the system, and thus the petroleum emplacement cannot affect the quartz growth (Bjørkum et al., 1998; Walderhaug, 1994). Some others argue that transport rates for aqueous species will be reduced and quartz precipitation rates will therefore be retarded or even be fully stopped (Marchand et al., 2001; Robinson and Gluyas, 1992; Worden et al., 1998). The hydrocarbon fluid inclusions occurred in quartz and were trapped when the hydrocarbon generation and migration suggest that quartz cementation continued after hydrocarbon emplacement (Baron et al., 2008). However, we draw this conclusion circumspectly, because there is no direct evidence shows quartz cementation rates were affected or unaffected by hydrocarbon. But the occurrence of fluid inclusion in the quartz suggests that the cementation continually destroyed the reservoir quality after it deeply buried and hydrocarbon emplaced. And this may be liable for the tight reservoir in the Yanchang Formation.

Conclusion

The thermal characteristics of the fluid inclusions in the quartz grains from Jiyuan area are coincident with the burial thermal history of the Yanchang Formation simulated from well, which implies that the thermal events occurred in the burial history of the Yanchang Formation may have a negligible record by the fluid inclusions in quartz.

The variation of salinity of the fluid inclusions depends on various factors. The regressions of salinity and burial depth suggest that the fluid interruption and dehydration reactions occurred in diagenetic processes, particularly in Chang 7 and Chang 8 members.

Quartz precipitation continued a long period in the Yanchang sandstones. Evidently, it starts before the buried depth approaching 1700 m. The process lasted until the deepest burial of the basin was reached, which covers about 60 Ma. Presumably, quartz cementation occurred more extensively than we described in this paper.

Evidence from fluid inclusion illustrated that the hydrocarbon generation occurred in the Jurassic and Cretaceous, and potential migration took place simultaneously. The tight reservoir may partially be ascribed to the quartz precipitation when the basin was deeply buried, coupling with the hydrocarbon accumulation.

Footnotes

Declaration of conflicting interests

The author(s) declared no potential conflicts of interest with respect to the research, authorship, and/or publication of this article.

Funding

The author(s) disclosed receipt of the following financial support for the research, authorship, and/or publication of this article: This study was supported by the National Natural Science Foundation for Young Scientists of China (Grant No. 41702123). We appreciate the help from the State Key Laboratory of Petroleum Resource and Prospecting for the fluid inclusion analysis, and we also thank the Changqing Oil Company for data supporting.

ORCID iD

Yunlong Zhang

References

Anovitz

Cole

Jackson

, et al. (2015) Effect of quartz overgrowth precipitation on the multiscale porosity of sandstone: A (U)SANS and imaging analysis. Geochimica Et Cosmochimica Acta 158: 199–222.

Baron

Parnell

Mark

, et al. (2008) Evolution of hydrocarbon migration style in a fractured reservoir deduced from fluid inclusion data, Clair field, west of Shetland, UK. Marine and Petroleum Geology 25(2): 153–172.

Bjørkum

Oelkers

Nadeau

, et al. (1998) Porosity prediction in quartzose sandstones as a function of time, temperature, depth, stylolite frequency, and hydrocarbon saturation. AAPG Bulletin 82(4): 637–647.

Bodnar

(1993) Revised equation and table for determining the freezing point depression of H₂O-NaCl solutions. Geochimica et Cosmochimica Acta 57(3): 683–684.

Brantley

Voigt

(1989) Fluids in metamorphic rocks: Effects of fluid chemistry on quartz microcrack healing in water-rock interaction. International Symposium on Water-Rock Interactions 6: 113–116.

Burley

Mullis

Matter

(1989) Timing diagenesis in the tartan reservoir (UK North-Sea): Constraints from combined cathodoluminescence microscopy and fluid inclusion studies. Marine and Petroleum Geology 6(2): 98–104.

Carr

Tester

(2013) Prediction of the solubility of quartz in salt solutions from 25°C to 900°C using the 3-parameter non-random two-liquid (NRTL) model. Fluid Phase Equilibria 337: 288–297.

Chen

Luo

Chen

, et al. (2006) Restoration of burial history of four periods in Ordos Basin. Acta Petrolei Sinica 27(2): 43–47. (in Chinese with English Abstract)

Chen

Guo

Jiang

, et al. (2017) Source rock characteristics and rock-eval-based hydrocarbon generation kinetic models of the lacustrine chang-7 shale of Triassic Yanchang formation, Ordos Basin, China. International Journal of Coal Geology 182: 52–65.

10.

Conliffe

Burden

Wilton

DHC

(2017) The use of integrated fluid inclusion studies for constraining petroleum charge history at parsons pond, Western newfoundland, Canada. Minerals 7(3): 39.

11.

Cui

Zhu

, et al. (2019) Development patterns of source rocks in the depression lake basin and its influence on oil accumulation: Case study of the Chang 7 member of the Triassic Yanchang formation, Ordos Basin, China. Journal of Natural Gas Geoscience 4(4): 191–204.

12.

Dai

Zou

Dong

, et al. (2016) Geochemical characteristics of marine and terrestrial shale gas in China. Marine and Petroleum Geology 76: 444–463.

13.

Dolníček

Kropáč

Janíčková

, et al. (2012) Diagenetic source of fluids causing the hydrothermal alteration of teschenites in the silesian unit, outer Western carpathians, Czech Republic: Petroleum-bearing vein mineralization from the stříbrník site. Marine and Petroleum Geology 37(1): 27–40.

14.

Dove

(1994) The dissolution kinetics of quartz in sodium chloride solutions at 25°C to 300°C. American Journal of Science 294(6): 665–712.

15.

Dove

Elston

(1992) Dissolution kinetics of quartz in sodium chloride solutions: Analysis of existing data and a rate model for 25°C. Geochimica et Cosmochimica Acta 56(12): 4147–4156.

16.

Dutton

Loucks

(2010) Diagenetic controls on evolution of porosity and permeability in lower tertiary Wilcox sandstones from shallow to ultradeep (200-6700 m) burial, Gulf of Mexico Basin, USA. Marine and Petroleum Geology 27(1): 69–81.

17.

Estupinan

Marfil

Delgado

, et al. (2007) The impact of carbonate cements on the reservoir quality in the Napo Fm sandstone (cretaceous Oriente Basin, Ecuador). Geologica Acta 5: 89–107.

18.

Ganor

Huston

Walter

(2005) Quartz precipitation kinetics at 180°C in NaCl solutions—Implications for the usability of the principle of detailed balancing. Geochimica et Cosmochimica Acta 69(8): 2043–2056.

19.

, et al. (2019) Source-rock evaluation and depositional environment of black shales in the Triassic Yanchang formation, Southern Ordos Basin, North-Central China. Journal of Petroleum Science and Engineering 173: 899–911.

20.

, et al. (2016) Characteristics of hydrothermal sedimentation process in the Yanchang formation, South Ordos Basin, China. Evidence from Element Geochemistry: Sedimentary Geology 345: 33–41.

21.

Hiatt

Kyser

Fayek

, et al. (2007) Early quartz cements and evolution of paleohydraulic properties of basal sandstones in three paleoproterozoic continental basins: Evidence from in situ δ18O analysis of quartz cements. Chemical Geology 238(1–2): 19–37.

22.

Kantorowicz

Bryant

Dawans

(1987) Controls on the permeability and distribution of carbonate cements in Jurassic sandstones: Bridgeport sands, Southern England, and Viking group, troll field, Norway. In: Marshall

JD (

ed.) Diagenesis of sedimentary sequences. Oxford: Blackwell, pp. 103–118.

23.

Karim

Hanley

Pe-Piper

, et al. (2012) Paleohydrogeological and thermal events recorded by fluid inclusions and stable isotopes of diagenetic minerals in lower cretaceous sandstones, offshore Nova Scotia, Canada. AAPG Bulletin 96(6): 1147–1169.

24.

Kuang

Huang

, et al. (2004) Change of terrestrial heat flow in Ordos Basin since late mesozoic and its effects on the pattern and evolution of the ecologic environment: Bulletin of mineralogy. Petrology and Geochemistry 23: 318–325.

25.

Kumar

Ghassemi

(2005) Numerical modeling of non-isothermal quartz dissolution/precipitation in a coupled fracture–matrix system. Geothermics 34(4): 411–439.

26.

Lan

Wang

Zhou

, et al. (2014) Impacts on sandstone reservoir quality of the third member of upper Triassic Yanchang formation, Penyang oilfield of Ordos Basin, China. Acta Petrologica Sinica 30(6): 1828–1840. (in Chinese with English Abstract)

27.

Lander

Larese

Bonnell

(2008) Toward more accurate quartz cement models: The importance of euhedral versus noneuhedral growth rates. AAPG Bulletin 92(11): 1537–1563.

28.

Zhou

, et al. (2016) Effect of organic matter on pore structure of mature lacustrine organic-rich shale: A case study of the Triassic Yanchang shale, Ordos basin, China. Fuel 185: 421–431.

29.

Duan

Chen

, et al. (2012) Albitization and hydrothermal diagenesis of Yanchang oil sandstone reservoir, Ordos Basin. Acta Petrologica et Mineralogica 31: 173–180. (in Chinese with English Abstract)

30.

Guzmics

Liu

, et al. (2011) Migration of immiscible hydrocarbons recorded in calcite-hosted fluid inclusions, Ordos Basin: A case study from Northern China. Russian Geology and Geophysics 52(11): 1491–1503.

31.

Luo

Liu

Lin

, et al. (2006) Impact of diagenesis and hydrocarbon emplacement on sandstone reservoir quality of the Yanchang formation (upper Triassic) in the Ordos Basin. Acta Geologica Sinica 80: 664–673. (in Chinese with English Abstract)

32.

Marchand

AME

Haszeldine

Smalley

, et al. (2001) Evidence for reduced quartz-cementation rates in oil-filled sandstones. Geology 29(10): 915–918.

33.

Milliken

Ergene

Ozkan

(2016) Quartz types, authigenic and detrital, in the upper cretaceous eagle ford formation, South Texas, USA. Sedimentary Geology 339: 273–288.

34.

O’Reilly

Shannon

Feely

(1998) A fluid inclusion study of cement and vein minerals from the Celtic Sea Basins, offshore Ireland. Marine and Petroleum Geology 15(6): 519–533.

35.

Osborne

Haszeldine

(1995) Reply to a discussion of ‘Evidence for resetting of fluid inclusion temperatures from quartz cements in oilfields’ by Osborne and Haszeldine (1993): Marine and Petroleum Geology 12(5): 570–575.

36.

Osborne

Haszeldine

(1993) Evidence for resetting of fluid inclusion temperatures from quartz cements in oilfields. Marine and Petroleum Geology 10(3): 271–278.

37.

Parnell

Carey

Monson

(1996) Fluid inclusion constraints on temperatures of petroleum migration from authigenic quartz in bitumen veins. Chemical Geology 129(3–4): 217–226. no

38.

Qiu

Liu

Mao

, et al. (2010) Enrichment feature of thorium element in tuff interlayers of upper Triassic Yanchang formation in Ordos Basin, China. Geological Bulletin of China 29: 1189–1191. (in Chinese with English Abstract)

39.

Ren

(1996) Research on the relations between geothermal history and oil-gas accumulation in the Ordos Basin. Acta Petrolei Sinica 17(1): 17–24. (in Chinese with English Abstract)

40.

Ren

Zhao

(1997) Late mesozoic comparative research on the geothermal field of the Ordos Basin and Qinshui Basin. Acta Sedimentologica Sinica 15(2): 134–137. (in Chinese with English Abstract)

41.

Ren

Cui

, et al. (2017) Thermal history and its controls on oil and gas of the Ordos Basin. Earth Science Frontiers 24(3): 137–148. (in Chinese with English Abstract)

42.

Ren

Zhang

Gao

, et al. (2007) Tectonic thermal history and its significance on the formation of oil and gas accumulation and mineral deposit in Ordos Basin. Science in China Series D-Earth Sciences 50(S2): 27–38.

43.

Ren

Zhao

Zhang

, et al. (1994) Research on paleotemperature in the Ordos basin. Acta Sedimentologica Sinica 12(1): 56–65. (in Chinese with English Abstract)

44.

Rimstidt

(1997) Quartz solubility at low temperatures. Geochimica et Cosmochimica Acta 61(13): 2553–2558.

45.

Rimstidt

Barnes

(1980) The kinetics of silica-water reactions. Geochimica et Cosmochimica Acta 44(11): 1683–1699.

46.

Ritts

Weislogel

Graham

, et al. (2009) Mesozoic tectonics and sedimentation of the giant polyphase nonmarine intraplate Ordos Basin, Western North China block. International Geology Review 51(2): 95–115.

47.

Robinson

Gluyas

(1992) Duration of quartz cementation in sandstones, North sea and Haltenbanken basins. Marine and Petroleum Geology 9(3): 324–327.

48.

Robinson

Grant

Oxtoby

(1992) Evidence against natural deformation of fluid inclusions in diagenetic quartz. Marine and Petroleum Geology 9(5): 568–572.

49.

Robl

Davis

(1993) Comparison of the HF-HCl and HF-BF₃ maceration techniques and the chemistry of resultant organic concentrates. Organic Geochemistry 20(2): 249–255.

50.

Rossi

Goldstein

Ceriani

, et al. (2002) Fluid inclusions record thermal and fluid evolution in reservoir sandstones, Khatatba formation, Western desert, Egypt: A case for fluid injection. AAPG Bulletin 86(10): 1773–1799.

51.

Schito

Corrado

Aldega

, et al. (2016) Overcoming pitfalls of vitrinite reflectance measurements in the assessment of thermal maturity: The case history of the lower Congo basin. Marine and Petroleum Geology 74: 59–70..

52.

Steele-MacInnis

Han

Lowell

, et al. (2012) The role of fluid phase immiscibility in quartz dissolution and precipitation in sub-seafloor hydrothermal systems. Earth and Planetary Science Letters 321–322: 139–151.

53.

Sterner

Bodnar

(1989) Synthetic fluid inclusions—VII: Re-equilibrium of fluid inclusions in quartz during laboratory-simulated metamorphic burial and uplift. Journal of Metamorphic Geology 7(2): 243–260.

54.

Taylor

Giles

Hathon

, et al. (2010) Sandstone diagenesis and reservoir quality prediction: Models, myths, and reality. AAPG Bulletin 94(8): 1093–1132.

55.

Walderhaug

(1994) Precipitation rates for quartz cement in sandstones determined by fluid inclusion microthermometry and temperature history modelling. Journal of Sedimentary Research 64(2): 324–333.

56.

Wang

C-Y

Sandvol

Zhu

, et al. (2014) Lateral variation of crustal structure in the Ordos block and surrounding regions, North China, and its tectonic implications. Earth and Planetary Science Letters 387: 198–211.

57.

Wang

Xin

Yang

, et al. (2014) Zircon SHRIMP U-Pb age and geological implications of tuff at the bottom of chang-7 member of Yanchang formation in the Ordos Basin. Science China Earth Sciences 57(12): 2966–2977.

58.

Wang

(2017) Ordos basin superposed evolution and structural controls of coal forming activities. Earth Science Frontiers 24(2): 54–63.

59.

Williams

Farver

Onasch

, et al. (2015) An experimental investigation of the role of microfracture surfaces in controlling quartz precipitation rate: Applications to fault zone diagenesis. Journal of Structural Geology 74: 24–30.

60.

Worden

Oxtoby

Smalley

(1998) Can oil emplacement stop quartz cementation in sandstones? Petroleum Geoscience 4(2): 129–137.

61.

(2008) Hydrocarbon generation and reservoir formation: A case from Chang 7 source rock in Majiatan area, west margin of Ordos Basin. Petroleum Exploration and Development 35(6): 657–663.

62.

Shi

Xie

, et al. (2016) Deep-lacustrine sandy debrites and turbidites in the lower Triassic Yanchang formation, southeast Ordos Basin, Central China: Facies distribution and reservoir quality. Marine and Petroleum Geology 77: 1095–1107.

63.

Yang

Zhang

(2005) Leading effect of the seventh member high-quality source rock of Yanchang formation in Ordos Basin during the enrichment of low-penetrating oil-gas accumulation: Geology and geochemistry. Geochimica 34(2): 147–154.

64.

Yang

Liu

(2013) Characteristics and resource prospects of tight oil and shale oil in Ordos Basin. Acta Petrolei Sinica 34(1): 1–11.

65.

Yang

(2002) Tectonic Evolution and Oil Gas Reservoirs Distribution in Ordos Basin. Beijing: Petroleum Industry Press. (in Chinese)

66.

Yang

Liu

Feng

(2016) Geochemical significance of 17 alpha(H)-diahopane and its application in oil-source correlation of Yanchang formation in Longdong area, Ordos Basin, China. Marine and Petroleum Geology 71: 238–249.

67.

Yang

(2005) Tectonic and stratigraphic controls of hydrocarbon systems in the Ordos Basin: A multicycle cratonic basin in Central China. AAPG Bulletin 89(2): 255–269.

68.

Zhang

Yang

, et al. (2006) Leading effect of high-class source rock of Chang 7 in Ordos Basin on enrichment of low permeability oil-gas accumulation: Hydrocarbon generation and expulsion mechanism. Petroleum Exploration and Development 33: 289–293.

69.

Zhang

Bao

Zhao

, et al. (2017) Origins of authigenic minerals and their impacts on reservoir quality of tight sandstones: Upper Triassic Chang-7 member, Yanchang formation, Ordos Basin, China. Australian Journal of Earth Sciences 64(4): 519–536.

70.

Zhao

jIN

Wang

Z L (2002) Investigation of oil-pool formation from the homogenization temperatures of fluid inclusions and biomarkers in reservoir rocks: A genetic model for the deng-2 oil-Pool in the Jiyuan depression. Marine and Petroleum Geology 19(9): 1141–1150.

71.

Zhou

, et al. (2016) Controls on reservoir heterogeneity of tight sand oil reservoirs in upper Triassic Yanchang formation in Longdong area, southwest Ordos Basin, China: Implications for reservoir quality prediction and oil accumulation. Marine and Petroleum Geology 78: 110–135.

72.

Zhu

Lin

Ren

, et al. (2015) Micro-fracture characteristics of tight sandstone reservoirs and its evaluation by capillary pressure curves: A case study of Permian sandstones in Ordos Basin, China. Journal of Natural Gas Science and Engineering 27(1): 90–97.

73.

Zou

Wang

, et al. (2012) Deep-lacustrine transformation of sandy debrites into turbidites, upper Triassic, Central China. Sedimentary Geology 265–266: 143–155.

74.

Zou

Zhang

Luo

, et al. (2010), Shallow-Lacustrine Sand-Rich Deltaic Depositional Cycles and Sequence Stratigraphy of the Upper Triassic Yanchang Formation. Ordos Basin: Basin Research, vol. 22, pp. 108–125.

75.

Zou

Zhao

Zhang

, et al. (2008) Formation and distribution of shallow-water deltas and Central-basin sandbodies in large open depression lake basins. Acta Geologica Sinica 82(6): 813–825. (in Chinese with English Abstract)

Fluid inclusions in buried quartz of the Yanchang sandstone in the Jiyuan area,Ordos Basin,China: Implications for basin evolution and petroleum accumulation

Abstract

Keywords

Introduction

Geological setting

Samples and methods

Results

Fluid inclusion petrography

Microthermometry and salinity

Vitrinite reflectance

Discussion

Geothermal history and fluid flow

Quartz precipitation

Petroleum implication

Conclusion

Footnotes

Declaration of conflicting interests

Funding

ORCID iD

References