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The main reservoir stratum of shale gas in the Jiaoshiba area, Sichuan basin is Wufeng-Longmaxi Formations. This paper calculates the tectonic difference stress values of JY1 well in different depths and numerically simulates the shale gas reservoir by elasto-plastic incremental method. The results of tectonic difference stress value suggest that the present tectonic stress values distribute strippedly in plane. The areas in favor of the development of fractures are stripped and mostly distributed in the northeast, middle and southwest of Jiaoshiba area, where the shale gas is concentrated.

The shale gas field in the Lower Silurian Longmaxi Formation in the Fuling, Sichuan Basin has been paid attention of the domestic and foreign scholars, which is the first shale gas field with one million cubic meters production. Some scholars suggest that the mud-shale reservoir is the main factor to affect the reservoir capacity and shale gas exploitation [

In recent years, many methods of cracks prediction are widely used, but finite element numerical simulation of the tectonic stress field is the most widely used [

There is a mud-shale reservoir enriched shale gas in the Lower Silurian Longmaxi Formation in the Jiaoshiba area, Fuling, Sichuan Basin. Therefore, we used elastic plastic incremental method to simulate the tectonic stress field in the Jiaoshiba area, predict the development of tectonic fractures and provide evidences for the favorable shale gas accumulation zones.

The Fuling shale gas field is located in Jiaoshiba, Fuling District of Chongqing City. Tectonically, this shale gas field is in the barrier type fold belt in the east of Sichuan Basin and the west of the Qiyueshan Fault, which is a special positive structure in the Wanzhou complex synclines (

Faulted anticline similar to a box shaped is the main tectonic in the Jiaoshiba area, which is different with narrow high steep anticlines along the both sides with NE or near NS trending. The Jiaoshiba structure is diamond shaped and boundaried by the two groups of reverse faults with NE and near NS trending respective, and separated by the fault-uplift, fault-depression with Qiyueshan Faults. The deformation of the Jiaoshiba structure is weak and the upper and lower tectonic layers are basically similar, which is like faulted anticline with box shaped, that is, relief top and small dip. Faults are not developed, while there are many faults in the steep flanks [

Because the present tectonic stress field is in the evolving, allocation and the formation process, those structure traces have not formed finally which can characterize the current tectonic stress field characteristics with a certain scale of permanent structure deformation. Therefore, the determination of the direction of modern tectonic stress is generally not by the geometry

At present, the methods are commonly used as following: analysis of the mechanism of natural earthquake, data of collapse in the engineering drilling, data of fault slip in the active faults and data of stress release in the borehole and so on.

Using natural earthquake focal mechanism solution method to determine the modern tectonic stress direction must be selected at the beginning of the earthquake or earthquake data, but can not use the aftershock data. After the formation of the earthquake, the aftershock, which usually only reflect a short-term, local stress state, can not be used as a parameter of the regional stress analysis. In recent decades, the domestic seismic network has been spread all over the country, and the method of solving the main stress direction with the focal mechanism is feasible and reliable.

Seismic source mechanism solution can be obtained by analyzing the seismic wave from the beginning to the record. In the process of seismic wave propagation, in each seismic station records with a seismic first arrival of the P wave (P-wave first motions of positive and negative (up and down) symbol and put them on the stereographic projection net, find out the classification of P wave first move plus and minus areas two faults (

Modern tectonic stress field maps of China have been compiled by the Crust Stress Research Institute of Chinese Academy of Sciences. The extrusion direction of Sichuan Basin is ca. SE120˚ in the modern tectonic stress field map of Sichuan Basin.

The modern tectonic stress field of Southern China suggests a direction of tectonic stress in a larger area. In order to the local direction of tectonic stress in the study area, we narrowed the scope of data collection and used the data of earthquake mechanism in the Jiaoshiba area, Sichuan Basin [

We calculated the the arithmetic average values of the 30 focal mechanism solutions and 15 drilling collapse data with result 122.98˚, which is consistent with the direction (SE120˚) of the main pressure stress of modern tectonic stress field of Southern China. Therefore, SE120˚ has been choiced as the the direction of the main pressure stress of modern stress field simulation.

We calculated the horizontal stress values in different depth (

No. | Abscissa | Ordinate | Earthquake date | Place | Orientation (˚) |
---|---|---|---|---|---|

1 | 18,347,157 | 3,432,122.4 | 2008/5/12 | Wenchuan, Sichuan | 283 |

2 | 18,387,483 | 3,477,862.3 | 2008/5/13 | Pengzhou, Sichuan | 288 |

3 | 18,327,963 | 3,426,869.8 | 2008/5/13 | Wenchuan, Sichuan | 289 |

4 | 18,327,066 | 3,471,255 | 2008/5/16 | Wenchuan, Sichuan | 276 |

5 | 18,490,549 | 3,569,626.7 | 2008/5/18 | Pingwu, Sichuan | 316 |

6 | 17,961,427 | 3,338,864.3 | 1989/4/25 | Eastern Batang, Sichuan | 264 |

7 | 17,974,099 | 3,340,478.8 | 1989/5/3 | Eastern Batang, Sichuan | 271 |

8 | 17,973,346 | 3,344,969.2 | 1989/5/3 | Eastern Batang, Sichuan | 260 |

9 | 17,967,872 | 3,331,868.8 | 1989/7/21 | Eastern Batang, Sichuan | 269 |

10 | 18,386,086 | 3,222,078.2 | 1994/12/30 | Mabian, Sichuan | 272 |

11 | 18,404,968 | 3,486,892.9 | 1958/2/8 | Maowen-Beichuan, Sichuan | 296 |

12 | 18,335,098 | 3,393,482.3 | 1970/2/24 | WesternDayix, Sichuan | 305 |

13 | 18,375,782 | 3,168,972.4 | 1970/7/31 | Northeastern Leibo, Sichuan | 305 |

14 | 18,380,956 | 3,196,632.6 | 1971/8/17 | Mabian, Sichuan | 316 |

15 | 18,380,979 | 3,198,849.5 | 1971/8/17 | Eastern Mabian, Sichuan | 354 |

16 | 18,375,947 | 3,184,490.7 | 1971/8/17 | Muchuan, Sichuan | 321 |

17 | 18,365,243 | 3,187,935.7 | 1971/8/18 | Eastern Mabian, Sichuan | 319 |

18 | 18,375,900 | 3,180,056.9 | 1971/8/23 | Eastern Mabian, Sichuan | 313 |

19 | 18,348,285 | 3,509,748.5 | 1933/8/25 | Northwestern Maowen, Sichuan | 274 |

20 | 18,363,030 | 3,165,789 | 1971/3/11 | Mabian, Sichuan | 297 |

21 | 18,373,054 | 3,187,847.7 | 1971/8/23 | Mabian, Sichuan | 308 |

22 | 18,392,684 | 3,198,735 | 1973/6/29 | Eastern Mabian, Sichuan | 265 |

23 | 18,366,219 | 3,187,924.4 | 1971/9/4 | Mabian, Sichuan | 286 |

24 | 18,373,175 | 3,198,932.4 | 1973/6/29 | Eastern Mabian, Sichuan | 301 |

25 | 18,361,364 | 3,190,198.7 | 1971/11/5 | Southern Mabian, Sichuan | 279 |

26 | 18,392,787 | 3,209,819.4 | 1974/12/30 | Mabian, Sichuan | 321 |

27 | 18,323,276 | 3,432,492.8 | 1976/2/15 | Wenchuan, Sichuan | 300 |

28 | 18,335,607 | 3,299,205.6 | 1973/12/30 | Southwestern Hongya, Sichuan | 284 |

29 | 17,977,516 | 3,310,252.1 | 1960/5/3 | Southeastern Batang, Sichuan | 283 |

30 | 18,118,645 | 2,892,441.3 | 1979/5/15 | Panxi, Sichuan | 277 |

No. | Abscissa | Ordinate | Depth | Place | Position (˚) |
---|---|---|---|---|---|

1 | 18,709,564 | 3,455,503.4 | 4441 | Guan 8 | 264 |

2 | 18,432,618 | 3,472,373.3 | 1985 | Chuanxi 106 | 280 |

3 | 18,605,965 | 3,480,788.6 | 937 | Chuanbei 57 | 280 |

4 | 18,597,714 | 3,468,399 | 2812 | Chuanbei 58 | 273 |

5 | 18,381,695 | 3,436,672 | 3405 | Chuanxi 95 | 286 |

6 | 18,436,653 | 3,212,487.4 | 2700 | Chuan 1 | 345 |

7 | 18,437,634 | 3,213,701.3 | 4325 | Chuan 2 | 335 |

8 | 18,438,599 | 3,212,033.5 | 0 | Chuan 3 | 345 |

9 | 18,440,504 | 3,277,977 | 0 | Chuan 4 | 355 |

10 | 18,441,462 | 3,275,976.7 | 2950 | Chuan 6 | 340 |

11 | 18,507,442 | 3,259,422 | 3025 | Chuan 7 | 340 |

12 | 18,520,469 | 3,244,363.6 | 2575 | Chuan 8 | 340 |

13 | 18,683,350 | 3,393,781.5 | 3775 | Chuan 11 | 330 |

14 | 18,414,404 | 3,478,827 | 2522 | Zhongba 46 | 315 |

15 | 18,724,802 | 3,346,636 | 1469 | Wo 89 | 278 |

No. | Layer | Depth (m) | Stress (MPa\MPa/ 100m ) | ||
---|---|---|---|---|---|

Overburden pressure | Maximum stress | Minimum stress | |||

JY1 | Longmaxi | 2380.70 | 58.62\2.46 | 63.50\2.67 | 47.39\1.99 |

Depth (m) | σ_{1} (MPa)_{ } | σ_{3} (MPa) | Δσ (MPa) |
---|---|---|---|

1800 | 48.041 | 35.848 | 12.193 |

2400 | 64.034 | 47.788 | 16.246 |

3000 | 80.054 | 59.728 | 20.326 |

3600 | 96.074 | 71.668 | 24.406 |

4200 | 112.094 | 83.608 | 28.486 |

4800 | 128.114 | 95.548 | 32.566 |

Young’s modulus and Poisson’s ratio are the necessary rock mechanical parameters in the numerical simulation of tectonic stress field by the elasto-plastic incremental method. The response for stress is different for different kinds of deformation medium. The deformation medium in the study area can be divided into two categories by the continuity: non continuous deformation medium and continuous medium deformation.

The fault is a non continuous medium. Stress releases in the faults and the difference stress values decrease during the numerical simulation of tectonic stress field by the elasto-plastic incremental method. Therefore, the scale of faults plays an important role in the current tectonic stress field. Then, the fault should be acted as a kind of deformation medium. For the fault as a non continuous deformation medium, the key point is in the time-depth conversion of seismic data. We got the depth sections from height −1800 m to height −4800 m, which include the fault tomographic point cutting this layer. In depth sections corresponding to the height-1800m however, Endo, these depth sections including wear fault tomographic point to this layer. These depth dections containing fault information are entered into DFDraw software. After coordinate correction of the depth sections and depiction of tomographic projection point, we got the distribution maps of faults corresponding to present simulation layers of tectonic stress (

The continuous deformation medium would influenced by stratigraphic age and sedimentary environment. The sedimentary environment in the Jiaoshiba area, Sichuan Basin is relatively single, that is, shallow shelf facies. So, three kinds of continuous deformation mediums have been divided in the Longmaxi-Wufeng Formation, the overlaying of Longmaxi-Wufeng Formation and Ordovician limestone underlaying the Longmaxi-Wufeng Formation (

The elastic modulus and Poisson’s ratio are the main parameters reflecting the characteristics of model material, which can be accurately determined in the testing machine of rock mechanics. Because these parameters would affect the simulation of plastic deformation process greatly during the mathematical simulations by this software, we must carefully select them. Generally, the measured data should be used as the first incremental elastic modulus and Poisson’s ratio, because these data are tested under the condition of elastic deformation. However, the elastic modulus would significantly decreas during the second, three and four incremental stage, then we can simulate the process of plastic deformation. But the Poisson’s ratio is just the opposite. Then, we should properly increase the Poisson’s ratio In order to simulate the plastic deformation. The maximum value of the Poisson’s ratio is 0.5, therefore Poisson’s ratio should not more than 0.45 even the presence of fault gouge or cataclasite.

The young’s modulus and Poisson’s ratio can be gotten from the shear wave logging data in the JY1 well of the study area. According to the small changes of the young’s modulus and Poisson’s ratio in different depths of JY1 well, average values of the young’s modulus and Poisson’s ratio in different depths would be taken as the simulation parameters (

Elastic plastic incremental method simulates the plastic deformation process of the geological body and tectonic stress field finite element numerically by increment method. After nearly 30 years of exploration and repeated trial, Chen Mingyou Professor and Wan Tianfeng Professor of China University of Geosciences established the elastic-plastic incremental method to finite element numerical simulate two-dimensional structure stress field.

The study of rupture deformation of rocks suggests that there are two deformation stages from the deformation to rupture of rocks, i.e. elastic deformation stage and plastic deformation stage. In the elastic deformation stage, stress is proportional to the deformation, which shows a straight line with a steeper slope in the stress & deformation map (

The elastic-plastic incremental method is characteristiced by the separation of the stress-deformation relationship in the plastic stage as many segments of linear, which are acted as a seires of elastic deformation process. This method can simulate the process of the rock deformation accurately. However, the majority of current mathematical simulation of stress field is only limited to simulate the elastic deformation. In fact, structural trace would not be produced in the elastic deformation. The rock will be restored with the removal of the stress.

Depth (m) | Property parameters | Above Longmaxi-Wufeng | Longmaxi-Wufeng | Ordovician limestone | Faults |
---|---|---|---|---|---|

1800 | Young’s modulus (MPa) | 4.04 | 3.36 | 3.534 | 2.69333 |

Poisson ratio | 0.274 | 0.314 | 0.274 | 0.411 | |

2400 | Young’s modulus (MPa) | 4.54 | 3.86 | 3.831 | 3.02667 |

Poisson ratio | 0.269 | 0.309 | 0.2265 | 0.4035 | |

3000 | Young’s modulus (MPa) | 5.04 | 4.36 | 4.331 | 3.36 |

Poisson ratio | 0.264 | 0.304 | 0.2215 | 0.396 | |

3600 | Young’s modulus (MPa) | 5.54 | 4.86 | 4.831 | 3.69333 |

Poisson ratio | 0.259 | 0.299 | 0.2165 | 0.3885 | |

4200 | Young’s modulus (MPa) | 6.04 | 5.36 | 5.331 | 4.02667 |

Poisson ratio | 0.254 | 0.294 | 0.2115 | 0.381 | |

4800 | Young’s modulus (MPa) | 6.04 | 5.36 | 5.331 | 4.02667 |

Poisson ratio | 0.249 | 0.289 | 0.2065 | 0.3735 |

External load force is applied around the designed geological model in order to produce the inner stress in the geological body, which is the key point of the numerical simulation of finite element structural stress field.

Generally, external load force should be evenly distributed around the model, in the best, evenly affect on the boundary line. However, when there are too many units with large grid density, it is convenient to apply a force on the node of the boundary of model and the accuracy is similar.

Generally, during the design of external load force on the boundary, it should be choised that the measured structural stress value with the same magnitude. The designed model should be approved when the direction of measured structural stress and the data of simulation are basically consistent in the model. However, it is difficult to achieve this goal unless repeated trial.

There are six numerical simulation layers in the study area (400 km^{2}), which are −1800 m, −2400 m, −3000 m, −3600 m, −4200 m and −4800 m isochronic lithology slices. We carried out the division of triangle units by four kinds of deformation media with different ages and different lithology. There are 15,546 of nodes, 354 of stress point of boundary, 2 constraint points of displacement and 3 times of increment.

Tectonic fractures form in the process of tectonic stress concentration and release. The fractures are not only depent on the size of tectonic stress, but also the release rhythm.

Some area is easy to the development of fractures where the stress gradient is relatively larger with the same stress value range [

The area with low stress value (blue) is the stress releasing area. In the difference stress contour map (

The area with low stress value (blue) is the stress releasing area. In the difference stress contour map (

The area with low stress value (blue) is the stress releasing area. In the difference stress contour map (

The area with low stress value (blue) is the stress releasing area. In the difference stress contour map (

The area with low stress value (blue) is the stress releasing area. In the difference stress contour map (

The area with low stress value (blue) is the stress releasing area. In the difference stress contour map (

The contour map of difference stress values by the simulation of the present tectonic stress field suggests that there is a large difference with the development of fractures in different depths. However, the areas in favor of the development of fractures are stripped and mostly distributed in the northeast, middle and southwest of Jiaoshiba area. Several areas are in the south east of the study area. These areas are close to the distribution of faults.

Unfortunately, the wells with hydraulic fracturing data in the Jiaoshiba area are not enough to complete the verification of simulation of the tectonic differential stress values. In addition, the regional stress field is so large by the elastic plastic incremental method in this study, and the data of sedimentary facies are relatively inaccurate, which affect the division of the type of media and the degree of sedimentary microfacies. Therefore, it is necessary to carry out the further study of the simulation and the prediction of fracture zone.

Qianqian Wang,Lu Wang, (2016) Prediction of the Favorable Area for the Development of Fracture in Mud-Shale of Wufeng-Longmaxi Formation in Jiaoshiba Area, Sichuan Basin. Open Journal of Geology,06,146-157. doi: 10.4236/ojg.2016.63014