Traditional Culture Encyclopedia - Traditional customs - Traditional Architecture in Western Henan Basin
Traditional Architecture in Western Henan Basin
(1) perfected the division and correlation marks of Paleogene, and divided five structural layers.
According to the principle of combining outcrop data with cover data, the division and correlation marks of pre-Paleogene are improved from lithostratigraphy, biostratigraphy, logging stratigraphy, seismic stratigraphy and comprehensive quantitative stratigraphy, and the structural layers are divided, and the remaining distribution of each structural layer is clear.
1. Traces of rocks and paleontology
Based on the main progress of lithostratigraphy and biostratigraphy, the standard fossils and rock marker beds of Paleogene in North China are systematically determined (Figure 7- 1), which fully reflects the research results of Paleogene in North China at present and provides a basis for the study of sedimentary formation. In addition, in view of the basin coverage area, this study also pays attention to the seismic reflection and logging curve response characteristics of strata, and finally determines the comprehensive indicators of each set of strata division.
Figure 7- 1 Paleogene fossils and rock marker beds in eastern North China
2. Sedimentary construction sequence and sedimentary discontinuity marks
Sedimentary formation and sedimentary discontinuity are comprehensive material records of Paleogene sedimentary tectonic environment and its evolution. Therefore, on the basis of new data, the sedimentary construction sequence and sedimentary discontinuity marks of Paleogene in North China are determined, and the characteristics of multi-cycle and multi-sedimentary discontinuity in Paleogene in North China are clarified.
Mesozoic-Neoproterozoic is a limited marine magnesium-rich carbonate with clastic rocks, and the top is missing Sinian system; The Lower Cambrian-Middle Ordovician is a set of sedimentary formations dominated by platform carbonate rocks. Upper Ordovician-Lower Carboniferous is missing; The Upper Carboniferous-Middle Triassic is a marine clastic sedimentary formation, and the Upper Triassic is missing. Jurassic and Cretaceous are sedimentary formations dominated by continental clastic rocks. There are many regional sedimentary discontinuities between the above sedimentary formations, which comprehensively reflect the evolution stages of Paleogene basins in North China.
3. Seismic response sign of stratum structure
The relationship between truncation and over-location of seismic reflection reflects the structural changes in the basin coverage area, which is one of the bases for determining the unconformity contact relationship and structural layer division of Paleogene. There are two main types of Paleogene in the eastern basin of North China: false conformity and unconformity. The false conformity contact relationship mainly appears between Neoproterozoic and Cambrian, Cambrian-Ordovician and Carboniferous-Permian, and the unconformity mainly appears between Mesoproterozoic and NeoArchean and within Mesozoic and Cenozoic.
4. For the Mesozoic "dumb layer", the method of multiple stratigraphic division is established.
In view of the Mesozoic "dumb strata" in the eastern part of North China, the multiple stratigraphic division method of "rock paleontology stratification, logging cycle subdivision and paleomagnetic dating (no paleontology)" is adopted to realize the stratigraphic division and correlation in the whole region, and it is clear that there is regional unconformity between the middle and upper Jurassic and the upper Jurassic-lower Cretaceous.
According to the above indicators, the Paleogene in North China is divided into five structural layers (Figure 7-2): structural layer 1 (basement), structural layer 2 (Mesoproterozoic), structural layer 3 (Cambrian-Ordovician), structural layer 4 (Carboniferous-Middle Triassic) and structural layer 5 (Jurassic-Cretaceous). This reflects the stages of tectonic development in North China Basin, and is the basis of basin nature and evolution analysis in each stage.
Figure 7-2 Structural Stratigraphic Division in the East of North China Basin
1-dolomite; 2- limestone; 3- shale; 4— Mudstone; 5- sandstone; 6— Gravelly complex sandstone; 7- Joint ventures; 8- basic volcanic rocks; 9- intermediate basic volcanic rocks; 10-tuff; 1 1- volcanic rocks; 12- almond basalt; 13- andesite basalt; 14-gneiss
The residual thickness of each structural layer changes greatly, which is mainly controlled by original sedimentation and later structural transformation. The second structural layer (Mesoproterozoic-Neoproterozoic) is affected by sedimentation and erosion, and distributed in the Liaoyan ancient trough, with a residual area of more than 20× 104 km2. The maximum settlement center is 6000 ~ 8000 m thick, distributed in Jixian, Lingyuan and a river, and becomes thinner to both sides. The area with a thickness greater than 1000m is greater than 13x 104km2. The residual thickness of the third structural layer (Cambrian-Ordovician) is 1 0,000 ~1200m, and its distribution is mainly controlled by fracture and erosion. The remaining thickness of Mesozoic-Cenozoic fault basin is relatively large, which is generally thick in the south and thin in the north, showing two high-value areas in the east and west and two low-value areas in the northeast alternately. The residual thickness of Carboniferous-Permian in the fourth structural layer (Carboniferous-Middle Triassic) is 800 ~ 1200m, and its distribution is controlled by faults and denudation, and it is distributed in two high-value areas in Northeast China, with the thickest in Nanpi Depression, Linqing area and Bozhong and Liaodong areas in central Hebei. The occurrence of Lower-Middle Triassic is similar to Carboniferous-Permian, but it is only distributed sporadically in the west of the study area, and the residual thickness can reach 2000 m m, with the center of residual thickness in Linqing and Huanghua Depression in the southwest. In the fifth structural layer (Jurassic-Cretaceous), the distribution of residual strata in the middle and lower Jurassic is mainly controlled by sedimentary depressions, and the sedimentary depressions in the south-central part of the study area are thick in the southeast and widely residual in the northwest. No deposition or sporadic distribution in other areas; Upper Jurassic-Cretaceous is distributed sporadically in the northwest of the study area, sporadically in the middle of the northwest and sporadically in the northeast, and its thickness varies greatly, reaching 3000 ~ 4000 m.
(2) The combination of point, line and surface restored the tectonic evolution of the basin.
According to the field observation of outcrop around Bohai Bay Basin 15 and the detailed anatomical analysis of about 200 seismic sections in this area, it is clear that there have been many structural styles such as compression, tension, strike-slip and inversion since Mesozoic, and the characteristics of multiple transformations of structural systems since Mesozoic are explained. Compressive structures were mainly formed in Indosinian and Yanshan ⅴ periods, extensional structures were mainly formed in Yanshan Ⅲ and ⅴ periods and early Cenozoic, strike-slip structures were mainly formed in Yanshan Ⅲ and Cenozoic, and two-phase inversion was mainly formed in Yanshan Ⅱ and early Cenozoic. Twenty-five seismic lines are selected for balanced profile analysis, and the extensional index in paleotectonic period is calculated, which well reflects the structural development, evolution process and regional stress field characteristics of the study area. The analysis shows that the pre-Mesozoic is characterized by overall rise and fall; Since Mesozoic, it has been generally characterized by the tectonic processes of upper Triassic compression, relative stability of middle-upper Jurassic, extension of upper Jurassic-lower Cretaceous, compression of upper Cretaceous and Paleogene-Quaternary extension, but there are differences in tectonic movement modes in different regions. Especially, the tectonic activity since Yanshan in the third act of Mesozoic controlled the strong anisotropy of different blocks.
According to the pre-Mesozoic basin and Mesozoic basin, different prototype basin restoration methods are adopted to restore the original sedimentary thickness in different periods. According to the geometric analysis of the basin, the kinematic characteristics of the marginal faults and internal faults in different periods and their controlling effects on the eastern North China basin are further discussed, and the evolution sequence of the Paleogene basin in the eastern North China is determined according to the principles of basin-mountain coupling, inheritance and regeneration, integrity and unity.
1. Rift craton Basin (Pt2+3)
The formation of craton basin is related to the development of rift in or around the basin. Lvliang Movement consolidated North China into an unbalanced craton; Since Mesoproterozoic, Chyi Chin and Xing 'an League were the north and south respectively. It went through the stages of division, diffusion and depression. The bottom is composed of continental clastic rocks and volcanic rocks rich in seismite, slump and turbidite deposits, while the upper part is composed of carbonate rocks and evaporite deposits with limited distribution and huge thickness. In the northern part of North China, the sedimentary centers are stably distributed in Jixian and Lingyuan, and the sedimentary thickness becomes thinner step by step to the northwest and southeast sides, and the Neoproterozoic sedimentary centers are slightly offset. The southern part of North China is dominated by clastic rocks, but a set of volcanic rocks can be seen at the bottom of western Henan, southern Shaanxi and Zhongtiaoshan, and the Neoproterozoic sedimentary center tends to expand eastward. Through basin correlation, the source rocks were mainly formed in the depression stage, and the Jixian system and Qingbaikou system have good structural conditions for the formation of source rocks.
2. Passive continental margin craton basin ()
The formation of craton basin is related to the development of passive continental margin on the basin edge, which is manifested by the coastal upwelling (from south to north, from north to south, from east to west) and the transformation of carbonate gentle slope to platform caused by sea level rise. Its sedimentary environment is an open ocean. The bottom is clastic rock and carbonate rock, containing terrigenous debris, and the top is carbonate rock, without terrigenous debris. The northern and southern parts of the basin have typical sequence characteristics of passive continental margin. The center of sedimentation and subsidence is at the edge of the basin. During this period, the source rocks are mainly distributed in the northern and southern margins of North China Basin, located at the bottom of Cambrian.
3. Active continental margin craton basin ()
The formation of craton basin is related to the development of active continental margin at the basin margin, which is manifested by the sea level drop at the basin margin caused by Huaiyuan movement (occasionally transgression caused by global sea level rise) and the transformation of carbonate platform to gentle slope. Its sedimentary environment is an isolated sea, evaporite deposits migrate from the edge to the center, and the sedimentary settlement center is in the center of the basin. During this period, the source rocks were mainly developed in the middle of North China Basin, and the source rocks were mainly distributed in Fengfeng Formation and Shangmajiagou Formation, and the limitations of the basin increased in the later period.
4. Convergence Craton Basin (C3-T 1+2)
The formation of craton basin is related to the convergence of basin margin, which is characterized by the development of marginal facies of basin margin, the broad and flat uplift area inside the basin and the deposition controlled by sea level change in the open sea. Its sedimentary environment is a kind of marginal sea, and the interior of the basin is shallow upward, and the continental deposits are constantly migrating to the edge of the basin. During this period, the source rocks were mainly distributed in the middle of North China Basin and developed in the intermittent transgression of benxi formation, Taiyuan and Shanxi Formations.
5. Intracontinental Flexural Faulted Basin (J+K)
The formation of the basin is related to the formation of the unified continent, which is characterized by the development of intraplate basins, strong division and changeable sedimentary and tectonic environment. Its sedimentary environment is fluvial facies and lacustrine facies, and the sedimentary and subsidence centers often migrate within the plate and often do not overlap. The middle and lower Jurassic is a flexural basin, and the upper Jurassic-lower Cretaceous is a faulted basin. The main dynamic mechanisms of basin subsidence are compression deflection and lithospheric detachment. The enrichment of source rocks is mainly related to local tectonic conditions and paleoclimate characteristics, among which the Lower Cretaceous has good hydrocarbon generation potential.
The universality of plate tectonic evolution and the particularity of North China basin evolution determine that it presents a complete cycle of craton basin evolution. The determination of the attributes of the North China Craton Basin is of great guiding significance to the oil and gas exploration of Paleogene in North China.
(3) Determine the distribution of the three major structural areas and their residual strata.
According to the analysis of fault distribution, activity characteristics and structural styles, combined with the distribution characteristics of residual strata, Bohai Bay Basin is divided into the east of Taihang Mountain, the west of Yanshan-Qikou-Xingang-Lankao-Liaocheng fault zone (type I structural zone), the east of Yanshan-Qikou-Xingang-Lankao-Liaocheng fault zone, the west of Tanlu fault zone (type II structural zone) and the north of Zhangjiakou-Penglai strike-slip fault zone.
Type I structural area is mainly characterized by the inherited development of NE-trending structure, and the residual strata are distributed in NE-trending direction, with the residual thickness center in the southeast. The NW-trending and NE-trending structures in Class II structural area are superimposed coherently, and the residual strata are distributed in NW direction, with the residual thickness center in the east. The NE strike-slip structure in class ⅲ structural area develops continuously, and the residual strata are distributed in NE direction, with the residual thickness center in the south.
(4) Propose and divide the Mesozoic and Cenozoic superimposed structural units in multi-cycle basins.
According to the characteristics of Bohai Bay Basin as a typical "China Basin", the concept of "superimposed structural unit" is put forward. On the basis of comprehensive consideration of Mesozoic and Cenozoic basins, six superimposed structural units are divided, namely, continuous subsidence type (Ⅰ), intermediate subsidence type (Ⅱ1), intermediate subsidence type (Ⅱ 2), intermediate subsidence type (Ⅲ), intermediate subsidence type (Ⅱ 4) and continuous uplift type (Ⅲ) (Figure 7-3).
Type I structural area: mainly composed of Mesozoic and Cenozoic inherited superimposed structural units of type I, III, II 2 and II 4; Type ⅱ structural area: Mesozoic and Cenozoic coherent superposition, with the development of type ⅰ, type ⅱ 1 and type ⅱ 2 superimposed structural units; Type ⅲ structural area: strike-slip zones are inherited and superimposed, and structural units ⅱ2, ⅱ3 and ⅲ are superimposed.
Superimposed tectonic units not only reflect the differences of tectonic evolution history of different tectonic units, but also reflect the differences of Paleogene thermal evolution history of different tectonic units, which may be an important controlling factor of primary oil and gas accumulation. From the burial history of residual strata and source rocks, it is considered that the new subsidence type (Ⅱ 2) in the middle period is the most favorable for the formation of primary oil and gas reservoirs, followed by the inherited subsidence type (Ⅰ) and the new subsidence type (Ⅱ 4) in the middle period. Therefore, superimposed structural units can be used as the main line of source rocks, reservoir-cap assemblage and reservoir formation research in strategic selection areas.
Figure 7-3 Plane zoning map of Mesozoic and Cenozoic superimposed structural units in eastern North China
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