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    准噶尔盆地腹部侏罗系超压特征和测井响应以及成因

    何生 何治亮 杨智 武恒志 王芙蓉 石万忠

    何生, 何治亮, 杨智, 武恒志, 王芙蓉, 石万忠, 2009. 准噶尔盆地腹部侏罗系超压特征和测井响应以及成因. 地球科学, 34(3): 457-470.
    引用本文: 何生, 何治亮, 杨智, 武恒志, 王芙蓉, 石万忠, 2009. 准噶尔盆地腹部侏罗系超压特征和测井响应以及成因. 地球科学, 34(3): 457-470.
    HE Sheng, HE Zhi-liang, YANG Zhi, WU Heng-zhi, WANG Fu-rong, SHI Wan-zhong, 2009. Characteristics, Well-Log Responses and Mechanisms of Overpressures within the Jurassic Formation in the Central Part of Junggar Basin. Earth Science, 34(3): 457-470.
    Citation: HE Sheng, HE Zhi-liang, YANG Zhi, WU Heng-zhi, WANG Fu-rong, SHI Wan-zhong, 2009. Characteristics, Well-Log Responses and Mechanisms of Overpressures within the Jurassic Formation in the Central Part of Junggar Basin. Earth Science, 34(3): 457-470.

    准噶尔盆地腹部侏罗系超压特征和测井响应以及成因

    基金项目: 

    教育部高等学校博士学科点专项科研基金 20060491505

    中国石化西部新区勘探指挥部项目 XBKY03-35

    国家自然科学基金重点项目 40739904

    详细信息
      作者简介:

      何生(1956-), 男, 教授, 博士生导师, 从事油气地质方面的教学和科研工作. E-mail: shenghe@cug.edu.cn

    • 中图分类号: P618.13;P631

    Characteristics, Well-Log Responses and Mechanisms of Overpressures within the Jurassic Formation in the Central Part of Junggar Basin

    • 摘要: 准噶尔盆地腹部地区深层钻井揭示侏罗系发育异常高压系统.根据26口井的67个钻杆测试(DST) 和电缆测试(MDT) 数据, 实测砂岩异常高压揭示深度约在4470~6160m, 剩余压力约为11~57MPa, 压力系数为1.24~2.07, 砂岩段超压实测值主要分布在侏罗系, 少数出现在白垩系底部与侏罗系邻近地层, 1个超压实测值位于下三叠统, 实测超压砂岩样品的孔隙度和渗透率范围分别为3.20%~16.00%和0.02×10-3~14.40×10-3μm2;根据钻井、测井和测试资料的综合解释, 埋深在4430~6650m的深部侏罗系流体超压带, 钻井泥浆密度明显增加, 泥页岩和砂岩共同具有相对于正常趋势的异常高声波时差和低视电阻率测井响应特征; 超压系统顶界埋深可能不浅于4400m (地温约104℃), 有些钻井超压顶界可深达约6000m (地温约140℃), 且超压带顶界深度随侏罗系埋深的增加而增大; 钻井揭示的侏罗系超压带烃源岩镜质体反射率(Ro, %) 约为0.7%~1.3%, 超压带分布深度受控于侏罗系成熟烃源岩层的埋深且两者深度分布的变化具有相关性; 研究认为腹部地区已被充分压实的侏罗系异常高压成因主要与其含煤岩系干酪根热演化及油气共生有关, 即生烃增压; 物理模拟实验表明, 由于高孔隙流体压力可导致岩石骨架颗粒间有效应力的减小, 从而直接引起通过岩石的声波速度降低, 即出现高声波时差响应; 在超压地层温度条件下, 高压液态水的电离常数可能明显增加, 从而减小地层电阻率, 进一步开展此种现象的相关探索性研究可望对超压带低电阻率异常的原因给出新的解释.

       

    • 图  1  准噶尔盆地腹部地区构造分区及研究钻井井位

      Fig.  1.  Map showing the tectonic subdivisions and the studied well locations in the central part of Junggar basin

      图  2  准噶尔盆地腹部地区钻井揭示地层厚度及相关信息

      Fig.  2.  Formation thicknesses and some related information from the boreholes in the central part of Junggar basin

      图  3  准噶尔盆地腹部地区实测地压、压力系数和地层水矿化度与深度的关系

      Fig.  3.  Profiles of measured pore pressures, pressure coefficients and total dissolved solids versus depth in the central part of Junggar basin

      图  4  ZHU1井测井泥岩、砂岩声波时差和视电阻率以及压力系数与深度关系

      Fig.  4.  Profiles of sonic, resistivity well-log data of mudstones and sandstones and pressure coefficients versus depth in the ZHU1 well

      图  5  PC2井测井泥岩、砂岩声波时差和视电阻率, 泥岩密度以及压力系数与深度关系

      Fig.  5.  Profiles of sonic and resistivity well-log data of mudstones and sandstones, density of mudstones and pressure coefficients versus depth in the PC2 well

      图  6  Y1井测井泥岩、砂岩声波时差和视电阻率以及压力系数对比

      Fig.  6.  Profiles of sonic, resistivity well-log data of mudstones and sandstones and pressure cefficients versus depth in the Y1 well

      图  7  D3井测井泥岩、砂岩声波时差和视电阻率以及压力系数对比

      Fig.  7.  Profiles of sonic, resistivity well-log data of mudstones and sandstones and pressure coefficients versus depth in the D3 well

      图  8  不同围压条件下饱含水砂岩样品(中砂岩, 总孔隙度19.08%、有效孔隙度14.75%) 的纵波速度与孔隙流体压力和有效应力关系的物理模拟实验(实验温度20 ℃) 结果

      Fig.  8.  Profiles of relationships between P-wave velocity and pore fluid pressure/effective stress using water saturated sandstone samples (middle sandstone, with a total porosity of 19.08% and effective porosity of 14.75%) within different conditions of surrounding pressures with the temperature of 20 ℃ from the results of physical simulation experiments

      表  1  准噶尔盆地腹部地区实测异常高压数据信息统计

      Table  1.   Measured data of overpressure and some related information in the study area

      表  2  实测超压井段中砂岩的实测孔隙度和渗透率以及岩性特征统计

      Table  2.   Measured porosity and permeability of sandstone samples in the overpressured layers

      表  3  准噶尔盆地腹部4口代表性井的超压顶界面的相关参数

      Table  3.   Parameters concerning the top of overpressure from the four wells in the central part of Junggar basin

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    • 收稿日期:  2008-10-21
    • 刊出日期:  2009-05-25

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