Qiao Xiufu Gao Linzhi Peng Yang Li Haibing

The original text was published in China Science (Series D) No.31Volume 200 1 Issue, and the English version was published in China Science (Volume 45, No.9, 2002). This paper discussed the earthquake disaster records and sequence stratigraphy (third-order sequence). Printed text figure 3 is replaced by color photos. 14 (the next chapter of this book) is the latest summary of the research on Dalin subgroups in recent years, and there are many new understandings. Some maps of 13 overlap with those of 14. In order to keep the original historical appearance and understanding at that time, the maps and descriptions in chapter 13 have not been deleted.

Canglang terrace of Lower Cambrian in Xuhuai area of Jiaoliao is distributed along both sides of Tanlu fault. Canglangpu terrace in Liaodong Peninsula includes Gejiatun Formation, Dalinzi Formation and Jianchang Formation (located on the east side of Tanlu Fault). Dalinzi Formation was formed in the coastal Sabha environment, and the whole rock stratum is full of earthquake disaster event records, which are manifested as liquefied drainage veins, water-plastic folds, water-plastic micro-faults (accompanied by the three), liquefied curl deformation, liquefied breccia and sandstone walls. The seismic liquefaction sequence of Sabha argillaceous rock is summarized. Canglangpu terrace in northern Jiangsu and Anhui (located on the west side of Tanlu fault) includes Jinshanzhai Formation, the lower member of Gouhou Formation and the upper member of Gouhou Formation. The Gouhou Formation is also a dry lagoon environment deposit, which belongs to the same climate zone rock stratum as the Dalinzi Formation, but no earthquake event record has been found in the terraced rock stratum in Canglangpu, northern Jiangsu and Anhui. Four sequences can be identified in Canglangpu terrace in northern Jiangsu and Anhui, and one sequence is missing in Liaodong Peninsula. From the perspective of catastrophic events, sequence stratigraphy and lithologic correlation of specific rock groups, the viewpoint that Canglangpu terrace system in Liaodong Peninsula moved from northern Jiangsu and Anhui to its present position in Mesozoic is not supported.

The ancient Tancheng-Lujiang belt (Figure 1) refers to southern Jilin, Liaodong Peninsula, central Shandong Peninsula and northern Jiangsu and Anhui. It is located in the east of China-Korea plate, and it is a strong intraplate earthquake zone in Neoproterozoic, which developed from Sinian to early Late Carboniferous.

Liquefied curl deformation and liquefied breccia liquefaction curl deformation refer to the inner layer curl caused by liquefaction (Figure 3D), which is a kind of flow plastic deformation [6]. Different from the reasons for the formation of dorsal and radial veins at both ends of liquefied argillaceous dolomite, dorsal and radial veins at both ends of argillaceous veins are formed by the puncture of argillaceous veins; The liquefaction deformation in the layer does not follow the mechanical mechanism and has no fixed law. Liquefied curl deformation can further develop into liquefied breccia. At the high tide of liquefaction, the rock stratum is torn and crushed in situ, forming breccia, which is collapsible. Liquefied drainage veins pierce the strata from different directions, making the strata brecciated, forming liquefied breccia, which is also collapsible.

The seismic liquefaction record of Dalinzi Formation consists of liquefaction drainage veins, liquid-plastic folds and liquid-plastic micro-faults (trinity) (see figure 2 14 in this book). It needs a certain seismic intensity to form the seismic records of each unit in the sequence of Dalinzi Formation. A statistical study on the data of water spraying and sediment discharge in the past 900 years before 1955 in China [7] shows that the magnitude is closely related to the liquefaction range, that is, the greater the magnitude, the greater the liquefaction range. When the magnitude is 6, the liquefaction range is about 10 ~ 50 km from the epicenter; When the magnitude is 7, the maximum distance from the liquefaction range to the epicenter is100 km; ; At magnitude 7.8, the liquefaction range is about 200 kilometers away from the epicenter (Tangshan earthquake on July 28th, 1976). The maximum distance between liquefaction range and the epicenter of destructive earthquake (1668 Tancheng M8.6 earthquake) is about 800km. However, when the earthquake magnitude is less than 5, there is no record of spraying water to remove sand in earthquake literature in China. Literature [8] has carried out a simulation experiment of sand layer vibration liquefaction, and selected the vibration frequency and acceleration of the area with earthquake intensity of 7 ~ 9 degrees (equivalent to earthquake magnitude above 6) to simulate the horizontal vibration during the earthquake, and the sand layer has been liquefied. Compared with historical earthquake records and simulation experiments, the earthquake magnitude that produces liquefaction needs to be above 5. Dalinzi Formation is located at the southern tip of Liaodong Peninsula, within 60 kilometers from Jinzhou Bay coast of Bohai Sea to Jinshitan coast of Dalian in the Yellow Sea in the eastern part of the Peninsula. The earthquake liquefaction record is very developed and spectacular. Therefore, Dalinzi Formation is a cataclysmic rock formation formed by strong earthquake in Early Cambrian.

2 sequence stratigraphy and correlation

Canglangpu terrace in Suxian County, northern Anhui Province includes Jinshanzhai Formation, the lower section of Gouhou Formation and the upper section of Gouhou Formation (Figure 2).

Regional geological survey team of Gouhou Formation of Anhui Geological Bureau. Three geological survey reports (1:200,000), including Dangshan Sheet (I-50-XV) in People's Republic of China (PRC). 1977, 1~60 1。

[9, 10] is actually divided into two sections. The lower member is the salt-bearing member of red clastic rock in arid environment. The lower part of the profile is interbedded with thin sandy shale and sandstone, the upper part is gravelly sandstone and the middle part is sandstone. There are abundant halite pseudocrystals and mud cracks in this layer. The lower member of Gouhou Formation is a barrier lake environment in arid climate zone. The horizon of this arid zone extends from northern Jiangsu and Anhui to northern Shandong to Liaodong (Dalinzi Formation) and southern Jilin (Heigouzi Formation) [5] (figure 1 8), and connects with the middle section of Houjiashan Formation (figure 1 7) to the south. The upper member of Gouhou Formation is limestone, which is equivalent to the limestone strata of Jiaochang Formation in southern Liaoning and Houjiashan Formation in Huainan [1 1].

The bottom boundary of Canglangpu Stage is the weathering crust of carbonate red soil at the top of the underlying Sinian system (namely Xingmincun Formation in Liaodong Peninsula, Shiwangzhuang Formation in Shandong Peninsula, Niyuan Formation in Suwan, Wangshan Formation, etc.). ). The top boundary is the discontinuous surface between the top of Alkali Factory Formation and Shantou Formation, and there are also weathered shells in most areas; The boundary between these two sequences is regional and can be traced back to the whole ancient Tancheng-Lujiang belt.

Four third-order sequences can be identified in the whole Canglangpu stage, namely Jinshanzhai Formation (DS 1), the lower member of Gouhou Formation (DS2) and the upper member of Gouhou Formation (DS4 DS3). The sequence interface between DS 1 and DS2 is a lithofacies transition surface. There is a carbonate transgressive hyperplane between DS3 and DS2, and DS2 is above DS 1 and DS2 clastic rock mats, which is the most important sequence interface of Canglangpu terrace. Fig. 2 In sequence stratigraphic correlation, sequence 3(DS3) is missing in Liaodong Peninsula, and DS4 directly exceeds DS 1 and DS2 clastic rock mats. In this paper, the Jinshanzhai Formation is placed in Cambrian from the point of view of the unconformity surface at the bottom of Canglangpu terrace and the clastic rock pad formed by Jinshanzhai Formation.

3 tectonic significance

The document [12] first puts forward that the Tanlu fault is a Mesozoic giant sinistral translation fault, and then comprehensively studies the Tanlu fault system1964 ~1996 [13 ~19], and considers that the translation fault distance reaches. This view has been widely valued and endorsed by many geologists at home and abroad [20 ~ 30]. According to the comparison of Neoproterozoic, Xu Xuesi systematically demonstrated that the middle part of the Tanlu fault (northern Jiangsu and Anhui and Liaodong Peninsula) was about 550 km to the left [29]. Chen Rongdu further proves from the geological comparison between Liaodong and western Liaoning (mainly from the strata and lithofacies belts in different periods) that the maximum translation distance of the Tanlu fault inferred by Xu Jiawei is 600 km [30]; They all think that the Neoproterozoic and Early Paleozoic basins in Liaodong Peninsula moved from northern Jiangsu and Anhui to their present positions.

Recent studies on the sinistral movement of the Tan-Lu fault tend to be late Jurassic or early Cretaceous [25,365,438+0], so the strata before Cretaceous in Liaodong Peninsula, including the Canglangpu stage involved in this paper, are distant systems, which have traveled long distances from Jiangsu and Anhui to their present positions. However, according to the research in this paper, the current Canglangpu stage lithostratigraphic record is contradictory to the viewpoint of giant translation.

(1) The strong earthquake record of Dalinzi Formation in Liaoning Peninsula was not found in Canglangpu step in the north of Jiangsu and Anhui, west of Tanlu fault. ① 1 in the picture is located on the east side of Liaodong Peninsula and along the coast of the Yellow Sea, and the Canglangpu seismic records are also distributed along the coast of Bohai Sea on the west side of the Peninsula. Liaodong Peninsula moves southward to the latitude position ⑤ in the map 1, and the distance between them is only 50 ~ 70 km. The liquefaction range of sediments during Canglangpu strong earthquake in early Cambrian should completely involve two areas. However, Canglangpu Steps in northern Jiangsu and Anhui lacked strong earthquake records, indicating that they were not in the same geographical position at that time.

(2) Canglangpu stage in Liaodong Peninsula is one sequence less than that in northern Jiangsu and Anhui. The third-order sequence has the significance of large-scale regional isochronous correlation, and there is no DS3 in Liaodong Peninsula, which indicates that there was regional tectonic uplift in Liaodong Peninsula after DS2 in Canglangpu period, and this uplift did not affect the northern part of Jiangsu and Anhui, indicating that the geographical positions of the two were far apart at that time.

(3) The lithology and lithofacies of Gejiatun Formation, Dalinzi Formation and Jianchang Formation are quite different from those of northern Jiangsu and Anhui (Figure 2).

4 conclusion

The above three points show that the Canglangpu terrace in the middle of the Tanlu fault in the east and south of Liaoning Province was not in the same geographical position as the Canglangpu terrace in the north of Jiangsu and Anhui (in the west of the Tanlu fault), and the Canglangpu terrace in Liaodong Peninsula could not be the result of the translation in the north of Jiangsu and Anhui. The seismic catastrophic events of Canglangpu stage and the objective geological records of sequence stratigraphy do not support the huge translation of Tanlu fault; Nor does it support the view that the Canglangpu stage in Liaodong Peninsula was a huge translation from northern Jiangsu and Anhui to the present position in the late Jurassic or early Cretaceous.

Canglangpu terraces in Liaodong Peninsula, northern Jiangsu and Anhui are distributed in NNE direction (Figure 1). Because they were formed in arid and semi-arid hot conditions, they are probably east-west basins parallel to the bottom of low latitude in Canglangpu period of Early Cambrian, and Canglangpu terraces in northern Jiangsu, Anhui and Liaodong are located at both ends of the basin.

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