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Comprehensive Provenance Analysis and Its Applications to Eocene Clastic Rocks in the Huimin Depression, Bohai Bay Basin, China

: Clariﬁcation of the source of the Eocene sediments ﬁlling the Huimin depression provides signiﬁcant support for current and future oil and gas exploration in the Bohai Bay Basin, China. A comprehensive assessment of sediment provenance based on sandstone petrography, heavy mineral assemblages, seismic reﬂection data, and distribution of sandstone bodies of the Shahejie Formation (Es 2 ) to the Dongying Formation (Ed) productive interval based on both its macroscopic and microscopic provenance aspects. This method of analysis has the advantages of easy data acquisition, high accuracy, strong ﬂexibility, wide application range, and making the analysis of sedimentary provenances more systematic. Comprehensive analysis of the Huimin depression, Bohai Bay Basin has revealed further that the origin of the Eocene second member of the Shahejie Formation (Es 2 ) to the Dongying Formation (Ed) provenance system was derived from the Linfanjia high, the Chengning uplift, and the Luxi uplift.


Introduction
Sediment provenance analysis plays an important role in determining sediment transport paths, the entire basinal depositional pattern, and prediction of the location of sand bodies in the basin [1]. Common provenance analytical methods include heavy mineral analysis, clastic petrography, geochemical analysis, and isotopic analysis [2]. Sedimentary models, such as the sand distribution system, mainly based on sedimentary principles, recognize that strata become thicker from the source area to the depositional center, thus determining the source of the sediments [3]. This method is maneuverable, and data are relatively easy to obtain, but due to the influence of the paleocurrent direction, provenance results can be limited and uncertain. Therefore, this method can only be used to judge the approximate direction of sediment transport near depositional areas, but not the actual location or the nature of the parent rock. Petrography can be used to infer the type of parent rocks in the source area based on the terrigenous clast assemblages in the basin [4]. Using Crook's (1974) connection between specific provenance areas and sedimentary basins in various tectonic environments, Dickinson et al. (1979) and Dickinson (1985) collected further data on the detrital components of sandstones in typical tectonic environments around the world, divided and quantitatively counted them in detail, and created provenance determination model maps, i.e., the Dickinson diagram [5][6][7][8]. The Dickinson diagram uses QtFL, QmFLt, QpLvLs, and QmPK model maps to place the provenance region in one of three main tectonic units and seven secondary tectonic units in stable continental

Materials and Methods
The mineralogical analyses were carried out using petrographic microscopes (Axioskop 40, ZEISS, Oberkochen, Germany). For this study, 182 thin sections and 471 heavy mineral concentrates prepared from clastic rocks were analyzed. Samples were collected from 13 wells in the study area. The 126 related sandstone thicknesses for various wells were determined after processing by using Gxplorer software (Version 3.0.3.0, Xi'an Gxplorer Software company, Xi'an, China). The 2D seismic profiles from 3D seismic data were analyzed at multiple angles, and three profiles with obvious reflection characteristics were selected for interpretation.
The comprehensive analysis method proposed in this paper can be used to extract provenance information by using microscopic analysis methods and macroscopic analysis methods ( Figure 1). We are performing assessment of sediments' sources. Compositional analysis of the clastic rocks was first determined using thin section, followed by lithologic assignment from compositional screening. The Gazzi-Dickinson counting method [24] was used to count, then, plot the compositional data on the Dickinson diagram to determine the tectonic setting history of the provenance. The main stable and unstable heavy minerals preserved in strata of the study area were screened from the target layer for Minerals 2019, 9,517 3 of 16 analysis. The variation of the ZTR index and the stability coefficient of the heavy minerals are indicators of the distribution of provenance exposures and can be used to identify those areas. According to the heavy mineral assemblage characteristics at different locations, the sedimentary regions can be subdivided and the parent rock lithologies identified. Based on the above results, we can deduce the sedimentary source regions. In order to prevent the omission of the source area, we need to discuss the results of analysis before proceeding with the macroanalysis. The analysis of the sandstone geometry (based on seismic reflections and bed thickness measured in drilling wells) provides complementary tools to establish sediment sources and dispersal paths in the basin sediment sources macroscopically. Based on the results of microscopic determination of the clastic rock composition and associated heavy minerals, the specific provenance can be verified by its progradation reflection characteristics on 2D seismic profiles. In addition, the progradation reflections on 2D seismic profiles with different angles further define the provenance direction and help to identify the provenance depositional system for the study area. With the aid of the planar variations in sandstone thickness, the range of influence of each provenance area on sedimentation can be determined ( Figure 1). Finally, the method identifies the provenance system for the study area. According to the heavy mineral assemblage characteristics at different locations, the sedimentary regions can be subdivided and the parent rock lithologies identified. Based on the above results, we can deduce the sedimentary source regions. In order to prevent the omission of the source area, we need to discuss the results of analysis before proceeding with the macroanalysis. The analysis of the sandstone geometry (based on seismic reflections and bed thickness measured in drilling wells) provides complementary tools to establish sediment sources and dispersal paths in the basin sediment sources macroscopically. Based on the results of microscopic determination of the clastic rock composition and associated heavy minerals, the specific provenance can be verified by its progradation reflection characteristics on 2D seismic profiles. In addition, the progradation reflections on 2D seismic profiles with different angles further define the provenance direction and help to identify the provenance depositional system for the study area. With the aid of the planar variations in sandstone thickness, the range of influence of each provenance area on sedimentation can be determined ( Figure 1). Finally, the method identifies the provenance system for the study area. The comprehensive provenance analysis method combines the advantages of petrology, heavy minerals, geophysics, and sedimentology, based on the microscopic provenance analysis of the clastic rock components and heavy minerals. The comprehensive provenance analysis method combines the advantages of petrology, heavy minerals, geophysics, and sedimentology, based on the microscopic provenance analysis of the clastic rock components and heavy minerals.

Regional Geologic Setting
The Huimin depression covers an area of about 5940 km 2 . It is bordered by the Shenxian depression to the west, the Dongying depression to the east, the Luxi uplift to the south, and the Chengning uplift to the north. The major axis of the depression is roughly NNE-trending and can be divided further into six fourth-level structural units: Linnan, Zizhen, Yangxin, Miaobei, Lizezhen, and Xiaozhuang ( Figure 2). Subsags and convex structures alternate within the Huimin depression, inclined from the south northward. The sedimentary succession in the Huimin depression mainly includes strata of Paleogene, Neogene, and Quaternary age. The Paleogene strata are the main oil-bearing interval, which include the Kongdian Formation (Ek), the Shahejie Formation (Es), and the Dongying Formation (Ed) (ascending order). The Shahejie Formation and the upper part of the Dongying Formation are exposed along the boundaries but are well preserved in the center of the subsidence zone, and the Neogene is unconformable with the Paleogene [25]. Among them, the Es, which is the main oil-producing interval, can be divided into four members: Es 1 , Es 2 , Es 3 , and Es 4 ( Figure 3). The lithologic successions are mainly siltstone and fine and medium grain sandstone.

Regional Geologic Setting
The Huimin depression covers an area of about 5940 km 2 . It is bordered by the Shenxian depression to the west, the Dongying depression to the east, the Luxi uplift to the south, and the Chengning uplift to the north. The major axis of the depression is roughly NNE-trending and can be divided further into six fourth-level structural units: Linnan, Zizhen, Yangxin, Miaobei, Lizezhen, and Xiaozhuang ( Figure 2). Subsags and convex structures alternate within the Huimin depression, inclined from the south northward. The sedimentary succession in the Huimin depression mainly includes strata of Paleogene, Neogene, and Quaternary age. The Paleogene strata are the main oilbearing interval, which include the Kongdian Formation (Ek), the Shahejie Formation (Es), and the Dongying Formation (Ed) (ascending order). The Shahejie Formation and the upper part of the Dongying Formation are exposed along the boundaries but are well preserved in the center of the subsidence zone, and the Neogene is unconformable with the Paleogene [25]. Among them, the Es, which is the main oil-producing interval, can be divided into four members: Es 1 , Es 2 , Es 3 , and Es 4 ( Figure 3). The lithologic successions are mainly siltstone and fine and medium grain sandstone. The basement structure of the Huimin depression is a tilted fault block, and the entire structure is an asymmetrical graben with a steep dip in the north, and a gentle dip in the south [26]. The Huimin depression has undergone four stages of deformation: (1) Initial rifting and subsidence in the Ek-Es 4 stage, (2) intense, deep subsidence in the Es 3 -Es 2 stage, (3) a second rifting stage, and (4) a shrinking An Early-Middle Triassic stable craton sedimentary stage was followed by denudation and uplift in the Late Triassic. From the Late Jurassic to the Cretaceous, the Yangxin area entered a stage of faulted basin development. The movement on all the faults in the Yangxin and Linnan subsags began the Linfanjia uplift and its associated denudation in the Paleogene (Figure 3). Due to uplifting, strata from the Es 2 to Ed were not developed on the Linfanjia high and deposition did not return until the Guantao formation (Ng) [27,28].

Type and Content
Based on the thin section analysis, the clastic rocks from Es 2 to Ed in the Huimin depression are mainly lithic feldspathic sandstones with less frequent feldspathic sandstones and feldspathic lithic sandstones ( Figure 4). The clastic rocks of the Es 2 , Es 1 , and Ed are similar, and there is no obvious vertical variation in rock type or detrital content. The quartz fraction volume is 30-60%, with an average volume of 44.22%. Most of the quartz is as single crystals, with a small amount of polycrystalline quartz. The plagioclase content is slightly higher than the K-feldspar content, and the The basement structure of the Huimin depression is a tilted fault block, and the entire structure is an asymmetrical graben with a steep dip in the north, and a gentle dip in the south [26]. The Huimin depression has undergone four stages of deformation: (1) Initial rifting and subsidence in the Ek-Es 4 stage, (2) intense, deep subsidence in the Es 3 -Es 2 stage, (3) a second rifting stage, and (4) a shrinking in the Es 1 -Ed stage. The evolution of the Huimin depression is controlled by regional tectonics. During the Neogene Period, the Luxi uplift and Chengning uplift were denuded due to the influence of fault activity.
An Early-Middle Triassic stable craton sedimentary stage was followed by denudation and uplift in the Late Triassic. From the Late Jurassic to the Cretaceous, the Yangxin area entered a stage of faulted basin development. The movement on all the faults in the Yangxin and Linnan subsags began the Linfanjia uplift and its associated denudation in the Paleogene ( Figure 3). Due to uplifting, strata from the Es 2 to Ed were not developed on the Linfanjia high and deposition did not return until the Guantao formation (Ng) [27,28].

Type and Content
Based on the thin section analysis, the clastic rocks from Es 2 to Ed in the Huimin depression are mainly lithic feldspathic sandstones with less frequent feldspathic sandstones and feldspathic lithic Minerals 2019, 9, 517 6 of 16 sandstones ( Figure 4). The clastic rocks of the Es 2 , Es 1 , and Ed are similar, and there is no obvious vertical variation in rock type or detrital content. The quartz fraction volume is 30-60%, with an average volume of 44.22%. Most of the quartz is as single crystals, with a small amount of polycrystalline quartz. The plagioclase content is slightly higher than the K-feldspar content, and the total integral of the plagioclase is 17-45%, with an average volume fraction of 32.51%. The lithics include metamorphic rocks, magmatic rocks, and a very small amount of sedimentary debris, contributing a volume that varies from 8-50% with an average of 23.10%.
Minerals 2019, 12, x FOR PEER REVIEW 6 of 16 total integral of the plagioclase is 17-45%, with an average volume fraction of 32.51%. The lithics include metamorphic rocks, magmatic rocks, and a very small amount of sedimentary debris, contributing a volume that varies from 8-50% with an average of 23.10%. From Es 2 to Ed, in order of decreasing abundance, the clastic rocks are mainly lithic feldspathic sandstones, feldspathic sandstones, and feldspathic lithic sandstones. The average mineral maturity (feldspar/quartz) is about 0.732 and the clastic rock grains exhibit medium sorting and secondary prismatic roundness in a particle support structure. Therefore, the detrital material did not undergo long-distance aqueous transport. According to its geological history, the uplift around the Huimin depression is likely to be the source area of the sediment.  From Es 2 to Ed, in order of decreasing abundance, the clastic rocks are mainly lithic feldspathic sandstones, feldspathic sandstones, and feldspathic lithic sandstones. The average mineral maturity (feldspar/quartz) is about 0.732 and the clastic rock grains exhibit medium sorting and secondary prismatic roundness in a particle support structure. Therefore, the detrital material did not undergo long-distance aqueous transport. According to its geological history, the uplift around the Huimin depression is likely to be the source area of the sediment.

Tectonic Setting of the Provenance Area
In this paper, five Dickinson ternary diagrams (QFL, QmFLt, QpLvLs, QmPK, and Lm (Lv + Lu) Ls) were plotted using the characteristics of the composition of the clastic rocks and their tectonic setting ( Figure 5).  Most of the samples on the QmPK ternary diagram fall into the strike-slip continental margin tectonic zone, which agrees with the geologic background of the Bohai Bay Basin and provides evidence of the accuracy of the other diagrams. Based on the QFL, Lm (Lv + Lu) Ls, and QmFLt ternary diagrams, most of the samples from the three study horizons fall in the dissected arc area and a small number of the samples fall in the basement uplift and mixed source areas. However, the QpLvLs ternary diagram show that all the samples fall into the dissected arc area. Therefore, we indicate that the provenance is the magmatic rock area. It is noteworthy that the QmFLt ternary diagram indicates the existence of a mixed source for the Huimin depression. Combined with the geologic background of the Huimin depression, the magmatic rock area which agrees with the Dickinson ternary diagrams, includes the Chengning uplift to the north and the Luxi uplift to the south of the Huimin depression, while the Linfanjia high could be the sediment source of the Es 2 , Es 1 , and Ed.

Heavy Mineral Data
Garnet, zircon, titanomagnetite, tourmaline, titanite, hornblende, pyroxene, chlorite, epidote, zoisite, and barite are the main heavy minerals recovered from strata with the Huimin depression. Stable heavy minerals account for more than 70% of the total heavy mineral content of the depression's clastic rocks. They have a high garnet and titanomagnetite content, and their stable heavy mineral assemblages are mainly garnet + zircon + titanomagnetite, indicating that the parent rocks were mainly magmatic and metamorphic.
Vertically, the ZTR index, the stability coefficient of the heavy minerals, and the heavy mineral assemblages in different layers of the same well do not change significantly from the Es 2 to the Ed. In the plane, the ZTR indices and the stability coefficients of wells P34, P3, P2, and P1 in the northwestern part of the depression (Area A) are lower than those of other parts (Figure 6a). Well XIA4 is located in the middle of the depression (Area C); the stability coefficient and the ZTR index in this well are the highest. For well M1, located in the northeastern part of the Huimin depression (Area D), both the ZTR index and the stability coefficient are lower than 20. From well L19 to well T3 to well T1 to well XIA4, from well S4 to S7 to XIA4, from M1 to XIA4, and from XIA1 to XIA4, the stability coefficient and the ZTR indices of the heavy minerals increase ( Figure 6). Thus, there may be five sedimentary supply directions: (1) A sedimentary source in the northwest represented by wells P34 and P3, (2) a NNW-trending provenance represented by the sediments of wells L19 and T3, (3) a northern provenance represented by the sediments of wells S4 and S7, (4) an eastern provenance represented by the sediments of well M1, and (5) a southern provenance represented by the sediments of well XIA4.
Combined with the tectonic setting, six sedimentary regions are defined based on their heavy mineral assemblages and mineral contents (Figure 7).

•
Area A It is represented by well P34. Its heavy mineral assemblage is garnet + zircon + titanomagnetite + tourmaline + titanite + epidote + zoisite. The titanomagnetite content of this area is >50%, the zircon content is 5%.

•
Area B Located in the northern part of the Huimin depression, Area B is represented by wells S4, T3, and L19. Its heavy mineral assemblage is garnet + zircon + titanomagnetite + tourmaline + chlorite + epidote + barite. The garnet content is the highest in this area, with an average content of 45%, while the average content of barite is 4%. The epidote and zoisite contents of Area B are lower than Area A. The Es 2 in wells 19 and S4 contains about 3% pyroxene. There are about 3% hornblende in the Es 1 and the Ed in well S7. In this area, when the pyroxene and hornblende contents increase, the chlorite content decreases.    • Area C It is represented by well XIA4. Its heavy mineral assemblage is garnet + zircon + titanomagnetite + tourmaline + titanite + epidote + barite. The zircon content increases, and it contains about 23% titanite.

•
Area D This is the Yangxin subsag, a fourth-level tectonic unit located in the eastern part of the Huimin depression, which is represented by well M1. Its heavy mineral assemblage is garnet + zircon + titanomagnetite + tourmaline + titanite + epidote + barite. The epidote content is very high, accounting for about 30% of the heavy minerals in each stratum, and the average content of garnet is less than 20%.
• Area E Located in the southern part of the Huimin depression, Area E is represented by well XIA1. Its heavy mineral assemblage is garnet + zircon + titanomagnetite + tourmaline + titanite + epidote + barite. The heavy mineral assemblage from this area is similar to that of Area D, but the epidote content is lower, and the titanomagnetite, zircon, and garnet contents are higher. Areas B and E are can be distinguished by their titanite content.

•
Area F Located in the western part of the Huimin depression, Area F is represented by well TANG2. Its heavy mineral assemblage is garnet + zircon + titanomagnetite + tourmaline + titanite + epidote + barite. Area F is distinguished from Area C by its mineral assemblage of garnet, titanomagnetite, and zircon almost of equal abundance, with each mineral accounting for about 30% of the total heavy mineral content.
According to heavy mineral assemblages, their contents and five sedimentary supply directions, we can conclude that the sediments in Area B are mainly sourced from north, Area E is mainly sourced from the south, and Area C is a mixed sedimentary area controlled by both the northern and south provenances. The sediments in Area A are controlled by the west of the Chengning uplift. The heavy mineral assemblage of Area F points to a mixed source. In well M1, from Area D, it indicates a provenance from the Linfanjia high, to the east of the depression. These data suggest that the Linfanjia high controls the sedimentation in the Yangxin subsag, but the influence of the Wudi high remains unclear.

Seismic Reflections
The progradation direction was sketched based on these seismic reflection features. There are obvious progradational reflection configurations in several of the seismic profiles of the target stratum in the study area (Figure 8). The sediments from the east, west, and south migrated to and accumulated in the depocenter of the Huimin depression.
2D seismic lines, 1620, 1162, and 1032, strike EW. Based on progradational reflection configurations, there are two directions of sediment supply, i.e., east and west. In the western part of 2D seismic section 1032, the characteristics of the progradation reflection are not obvious. The area of the source region to the east of the Huimin depression might be larger than the western provenance area. The eastern provenance area is the Linfanjia high, and the western provenance area is the west of the Chengning uplift.
2D seismic lines, 1215, 1638, 2215, and 2415, strike NS. Seismic profiles 1638 and 2215 have obvious progradational reflection configurations. From west to the east, debris was supplied to the sedimentary center from the southern and northern parts of the Huimin depression. The provenance of the depression is multidirectional. Overall, the southern provenance system has the western part of the Luxi uplift as its core, and the northern provenance system has the Chengning uplift as its core. These two provenances are the main sediment source areas for the Huimin depression.

Seismic Reflections
The progradation direction was sketched based on these seismic reflection features. There are obvious progradational reflection configurations in several of the seismic profiles of the target stratum in the study area (Figure 8). The sediments from the east, west, and south migrated to and accumulated in the depocenter of the Huimin depression. 2D seismic lines, 1620, 1162, and 1032, strike EW. Based on progradational reflection configurations, there are two directions of sediment supply, i.e., east and west. In the western part of 2D seismic section 1032, the characteristics of the progradation reflection are not obvious. The area of the source region to the east of the Huimin depression might be larger than the western provenance area. The eastern provenance area is the Linfanjia high, and the western provenance area is the west of the Chengning uplift.
2D seismic lines, 1215, 1638, 2215, and 2415, strike NS. Seismic profiles 1638 and 2215 have obvious progradational reflection configurations. From west to the east, debris was supplied to the sedimentary center from the southern and northern parts of the Huimin depression. The provenance of the depression is multidirectional. Overall, the southern provenance system has the western part of the Luxi uplift as its core, and the northern provenance system has the Chengning uplift as its core. These two provenances are the main sediment source areas for the Huimin depression.

Distribution of Sandstone Bodies
Isopach maps of the sandstone bodies were drawn (Figure 9). From the Es 2 to the Ed, the sedimentary center of the sand body migrated westward. The thickness of the Es 2 sand body gradually increases from the northwest, east, southwest, and south to the center of the depression. The Es 1 sand body in the mid-western part of the Huimin depression has obviously been thickened. The thickness of the sand body, which is centered on well XIA28, decreases gradually from west to

Distribution of Sandstone Bodies
Isopach maps of the sandstone bodies were drawn (Figure 9). From the Es 2 to the Ed, the sedimentary center of the sand body migrated westward. The thickness of the Es 2 sand body gradually increases from the northwest, east, southwest, and south to the center of the depression. The Es 1 sand body in the mid-western part of the Huimin depression has obviously been thickened. The thickness of the sand body, which is centered on well XIA28, decreases gradually from west to east. Compared with Es 1 , the sand body in Ed is thickened in the mid-western part of the depression. The sand body is thickened from the northwest, north, east, and south to the mid-western part of the depression in the form of a leaf. In general, there are four directions of sediment supply: Northwest, north, south, and east. The thickness of the sand body in the northern part of the Huimin depression spreads toward the center in the form of a leaf, so there should be many subordinate provenances to the north of the Huimin depression. There is a thicker sand body in the northeastern part of the depression, which should be the sedimentary sand body controlled by the provenance to the east of the depression.
The sand body is thickened from the northwest, north, east, and south to the mid-western part of the depression in the form of a leaf. In general, there are four directions of sediment supply: Northwest, north, south, and east. The thickness of the sand body in the northern part of the Huimin depression spreads toward the center in the form of a leaf, so there should be many subordinate provenances to the north of the Huimin depression. There is a thicker sand body in the northeastern part of the depression, which should be the sedimentary sand body controlled by the provenance to the east of the depression.

Discussion
As has been mention above, lithologically, the clastic rocks of the Huimin depression are mainly lithic feldspathic sandstones exhibiting low maturity and a short distance of fluvial transport, the Chengning and Luxi uplifts conform to the tectonic setting of a dissected arc belt indicated by Dickinson diagrams, and, depositionally, the sediments from Chengning and Luxi uplifts entered the depocenter from different angles. Therefore, we conclude that there should be multiple source outlets and multiple watercourses in the north and south of the Huimin depression and there are two source areas, i.e., the Luxi uplift and the Chengning uplift. Due to the influence of faults, the provenance system to the north is both complex and multidirectional. The northern provenance area can be divided into two secondary provenance systems based on six areas of sedimentation. These are the western secondary system to the west of the Chengning uplift, and the middle secondary system represented by the Chengning uplift. The northern provenance of system-controlled sedimentation is subdivided into the Xiaozhuang, Tangzhuang, Linyi, Jishan, Shanghe, and Zizhen regions. The dip of strata to the south of the Huimin depression is relatively gentle, and its provenance system mainly controls sedimentation in the Linnan subsag. The Yangxin subsag in the eastern part of the Huimin depression is weakly influenced by both northern and southern provenance systems.
In addition, the amount of erosional denudation suffered by the Ningjin high is about 50% of the total sedimentary volume of the entire Ek, Es, and Ed intervals in the northwestern part of the Huimin depression [29]. The Dickinson ternary diagram indicates that there are other provenances in addition to the dissection island arc area. The east-west 2D seismic section across the middle of the depression shows that there is a provenance system to the east. The stability of the heavy minerals gradually increases from the eastern part of the depression to the central part of the depression, and the unstable heavy mineral epidote accounts for a large proportion of the eastern sediments. The sedimentary sand body has another depocenter in the northeastern part of the Huimin depression. Therefore, there is the other sediment source area except the Luxi and Chengning uplifts for the basin-fill. The Linfanjia high to the east of the Huimin depression gradually became involved in the sedimentation of the Shahejie Formation and reached stability in the Es 2 . The sedimentary strata affected by the Linfanjia high are mainly the lower member of the Es 2 , so it could be the sediment source of the Es 2 , Es 1 , and Ed. The early sediments of the Linfanjia high were derived from the Chengning uplift to the north and the Luxi uplift to the south. Therefore, the tectonic setting may show a dissection arc, which agrees with the results of the Dickinson ternary diagrams. By combining the comprehensive provenance analysis method with the geological background, we identify the Linfanjia high, which is located to the east of the Huimin depression, as the third largest provenance area of the Huimin depression. The sand of well S971 is thick, and 158 meters of sand was deposited during the Ed period. The thickness of sand to the east of well S971 is thinner, so we conclude that the Linfanjia controls the sedimentation of the Yangxin subsag. The influences of the Wudi high on the Yangxin subsag are not clear. Wang (2007) analyzed the provenance of the Es 3 in the Huimin depression using the ratios of characteristic elements [29]. The analysis shows that the Mg/Mn ratio of the sedimentary strata is high, which is consistent with the characteristic element ratios of the Precambrian gneiss and some of the Ordovician strata in the Chengning and the Luxi uplifts. The Mg/Mn ratio of the sediments in the Es 2 is high, like that of the Precambrian magmatic and metamorphic rocks of the Chengning uplift and the Luxi uplift [23]. Furthermore, in accordance with the results of that analysis, we can conclude that the provenance of the Es 2 , Es 1 , and Ed in the Huimin depression is mainly magmatic and metamorphic rocks. Thus, the Precambrian and Ordovician strata in the Chengning and Luxi uplifts might be the sedimentary source of sedimentary strata of units Es 2 , Es 1 , and Ed in the Huimin depression. In order to further explore the age information of the parent rock, zircon can be used for dating.

Conclusions
Based on the geological background, the comprehensive analysis of the rock composition, heavy minerals, sand distributed system, and seismic reflection characteristics, three conclusions can be drawn.
The sediment sources of the Es 2 , Es 1 , and Ed in the Huimin depression were analyzed using comprehensive provenance analysis method. We concluded that there are two provincial areas, i.e., the Luxi uplift to the south and the Chengning uplift to the north of the Huimin depression.
The provenance system of the Chengning uplift to the north is the more complex multi-directional source. The Chengning system can be divided into two major provenance systems, the western and central systems. The system has two main provenance directions, northwest and north, and contains multiple secondary provenance directions. The western sub-provenance system controls sedimentation in the Xiaozhuang and Tangzhuang areas of the northwestern part of the Huimin depression, while the central sub-provenance system controls sedimentation in the Linyi, Jishan, and Shanghe areas. The southern Luxi uplift provenance system consists mainly of the southwestern provenance system. The southwestern provenance system mainly controls sedimentation in the southern slope belt of the Huimin depression.
By applying the comprehensive provenance analysis method, we concluded that the provenance area is the Linfanjia high to the east of the Huimin depression. The Linfanjia high controls the sedimentation of the Yangxin subsag.
Author Contributions: As the corresponding author, H.W. made substantial contributions to the conception/design of the work; he has approved the final version to be published; and he agrees to be accountable for all aspects of the work in ensuring that questions related to the accuracy or integrity of any part of the work are appropriately investigated and resolved. Following H.W. designs, Z.Z. performed all the experiments, analyzed experimental results, and drafted the work. Z.Z. and H.W. provided important intellectual support in interpretation of the data and discussion; all authors critically revised the manuscript.
Funding: This research received no external funding.