东丽湖地热钻探CGSD01井钻完井技术

CGSD01井是由中国地质调查局组织实施的一口水热型地热资源调查井。该井完井深度405168 m,终孔直径216 mm。施工过程中遇到大直径套管下入安全系数不足、地层漏失、复杂地层岩心采取率低等问题。文章介绍了该井的井身结构设计、钻完井工艺技术。通过采用浮力法下管,多工艺堵漏,改进复杂地层取心工艺等措施解决了施工过程中的复杂问题,总结了该地区深部地热钻探钻井工艺并提出了完井建议。     

“小而肥”油藏油水分布特征及成因探讨——以海拉尔贝尔凹陷贝中油田为例

针对“小而肥”油田油气成藏特点,以贝尔凹陷贝中油田为例,在对其探评井及开发井测井曲线、地震解释成果、测井解释资料、试油试采动态开发数据研究整理的基础上,结合其断裂系统拆分结果,通过典型实例分析和油藏解剖得知,贝中油田南一段主力油层在“满凹含油”的基础上,形成含油性差区或水区的主要控制因素为:断层断失作用造成目的层内主力...     

鲁西地壳隆升的伸展构造模式

伸展链锁断层系，形成了鲁西的主导造格局，即“块断”构造。它是由中、生代两次伸展运动形成的。伸展运动幔源岩浆活动有着密切的成生联系。伸展运动的结果，形成了以泰山－鲁山－沂山为核心的鲁中块隆，它至今耸立于周围以平原地貌为标志的地堑系之间，隆起的高点，就是当今的泰山。     

鄂尔多斯盆地子洲气田上古生界山西组、下石盒子组储集层特征对比研究

鄂尔多斯盆地子洲气田山西组山2~3段和下石盒子组盒8段是该区天然气的主力储集层,但其产能却存在很大差异。应用薄片鉴定、扫描电镜、高压压汞、恒速压汞及岩心分析资料,分别对该地区上古生界山西组山2~3段和下石盒子组盒8段储集层进行了研究。子洲气田山2~3储层以石英砂岩为主,孔隙类型多样,粒间孔、溶孔、晶间孔发育,喉道类别以微—细喉为主,属相对低孔高渗型储层;盒8储层则以岩屑砂岩为主,孔隙类型主要为岩屑溶孔和晶间孔,喉道类别以细—微喉为主,属于相对低孔低渗型储层。山2~3段和盒8段储集层岩石类型、孔隙结构差别巨大,造成了其储集性能的差异性。不同的沉积环境和成岩作用是造成其差异性的主要原因。     

Cases-97: Late-Morning Warming And Moistening Of The Convective Boundary Layer Over The Walnut River Watershed

Aircraft, radiosonde, surface-flux, and boundary-layer windprofiler data from the Cooperative Atmosphere Surface Exchange Study's 1997 field project, CASES-97, are combined with synoptic data to study the evolution of the vertically-averaged mixed-layerpotential temperature []and mixing-ratio [Q] onthree nearly-cloudless days from 1000 CST to 1200CST (local noon is approximately 1230 CST). This was achieved through examination of the terms in the time-tendency (`budget')equations for []and [Q]. We estimate three of the terms –local time rate of change, vertical flux divergence, andhorizontal advection. For the [Q]-budget, vertical flux divergence usually dominates, buthorizontal advection is significant on one of the three days. The [Q]-budget balances for two of the three days to within the large experimental error. For the -budget,vertical flux divergence accounts for most of the morningwarming, with horizontal advection of secondary importance.The residual in the -budget has the same sign for all three days, indicating that not all the heating is accounted for. We can balance the []-budgets to within experimental error on two of the three days by correcting the vertical-flux divergence for apparent low biases in the flux measurements of one of the aircraft and in the surface fluxes, and accounting for direct heating of the mixed layer by radiative flux divergence allowing for the effects of carbonaceous aerosols. The [];-budget with these corrections also balances on the third day if horizontal gradients from synoptic maps are used to estimate the horizontal advection. However, the corrected budget for this day does not balance if the horizontal gradient in the advection term is estimated using CASES-97aircraft and radiosondes; we suggest that persistent mesoscale circulations led to an overestimate of the horizontal gradient andhence horizontal advection.     

SIMULATION OF BOUNDARY LAYER EFFECTS ON A HEAVY RAINFALL EVENT CAUSED BY A MESOSCALE CONVECTIVE SYSTEM OVER THE YELLOW RIVER MIDSTREAM AREA

A heavy rainfall event caused by a mesoscale convective system (MCS), which occurred over the Yellow River midstream area during 7–9 July 2016, was analyzed using observational, high-resolution satellite, NCEP/NCAR reanalysis, and numerical simulation data. This heavy rainfall event was caused by one mesoscale convective complex (MCC) and five MCSs successively. The MCC rainstorm occurred when southwesterly winds strengthened into a jet. The MCS rainstorms occurred when low-level wind fields weakened, but their easterly components in the lower and boundary layers increased continuously. Numerical analysis revealed that there were obvious differences between the MCC and MCS rainstorms, including their three-dimensional airflow structure, disturbances in wind fields and vapor distributions, and characteristics of energy conversion and propagation. Formation of the MCC was related to southerly conveyed water vapor and energy to the north, with obvious water vapor exchange between the free atmosphere and the boundary layer. Continuous regeneration and development of the MCSs mainly relied on maintenance of an upward extension of a positive water vapor disturbance. The MCC rainstorm was triggered by large range of convergent ascending motion caused by a southerly jet, and easterly disturbance within the boundary layer. While a southerly fluctuation and easterly disturbance in the boundary layer were important triggers of the MCS rainstorms. Maintenance and development of the MCC and MCSs were linked to secondary circulation, resulting from convergence of Ekman non-equilibrium flow in the boundary layer. Both intensity and motion of the convergence centers in MCC and MCS cases were different. Clearly, sub-synoptic scale systems in the middle troposphere played a leading role in determining precipitation distribution during this event. Although mesoscale systems triggered by the sub-synoptic scale system induced the heavy rainfall, small-scale disturbances within the boundary layer determined its intensity and location.     

夏季亚洲季风区对流层向平流层输送的源区、路径及其时间尺度的模拟研究

基于NCEP/NCAR分析资料和拉格朗日轨迹输送模式FLEXPART, 通过气块轨迹计算, 对2005年夏季亚洲季风区对流层向平流层输送 (Troposphere to Stratosphere Transport, 简称TST) 的近地层源区、 输送路径及其时间尺度问题进行了一些初步探讨。结果表明: (1) 夏季亚洲季风区TST两个主要的边界层源区, 一个是热带西太平洋地区; 另一个是青藏高原南部、 孟加拉湾以及印度半岛中北部等地区, 上述两个区域与夏季强对流的分布相一致。在对流层顶高度附近 (约16 km高度), 两个近地层源区的垂直输送贡献相当。但进一步分析发现, 穿越对流层顶高度的质量输送只有约10％能够进入20～22 km高度的平流层中, 且主要源于以青藏高原南侧为代表的南亚季风区 (约贡献75%), 这进一步强调了青藏高原及其周边区域在全球TST过程中的重要地位。 (2) 轨迹分析显示, 夏季亚洲季风区对流层进入平流层的 “入口区” 主要在 (25°N～35°N, 90°E～110°E) 区域的青藏高原及其周边区域。TST路径受对流层上层南亚高压闭合环流、 北半球副热带西风急流和赤道东风急流的共同控制。 (3) 亚洲季风区TST两个主要的过程, 一个是和夏季湿对流抬升直接联系的快速输送过程, 它可以使近地层大气在1～2天内输送到平流层中, 贡献了整个TST的10%～30%; 另一个是大气辐射加热所致的大尺度垂直输送, 该输送是一个相对的慢过程, 时间尺度一般为5～30天。此结果意味着, 源于地表的短生命周期的大气污染物可通过光化学反应过程对该区域平流层臭氧及其他大气痕量成分平衡产生重要影响。     

一次梅雨锋结构及锋区强度对锋面结构影响的数值模拟

利用中尺度模式MM5对1999年6月下旬发生在长江中下游地区的一次锋上西南低涡发展的梅雨锋暴雨过程进行了研究。通过敏感性试验, 探讨了低涡对锋强、 锋生的敏感性, 锋生、 锋消与低涡发展演变的时间空间上的联系等问题\.结果表明, 低涡对中层锋面强度的变化敏感, 中层锋强发生改变会导致整层涡度发生同位相的变化。中层系统对梅雨锋气旋的发展起主要作用, 中层锋面对低涡发展的影响比边界层锋更关键。中层锋面强度改变会激发出中低层的垂直次级环流, 低层的辐合上升运动发生改变, 最终影响到低涡强度的发展。敏感性试验证明, 锋面强度变化对低涡发展造成的影响有超前性, 中层锋面先发生变化, 6 h左右以后低涡强度发生改变。锋区强度和低涡强度发生变化的地理位置基本在同一经度上, 锋强变化的位置在涡强变化位置的北面。     

Role of horizontal density advection in seasonal deepening of the mixed layer in the subtropical Southeast Pacific

The mechanisms behind the seasonal deepening of the mixed layer(ML) in the subtropical Southeast Pacific were investigated using the monthly Argo data from 2004 to 2012. The region with a deep ML(more than 175 m) was found in the region of(22?–30?S, 105?–90?W), reaching its maximum depth(～200 m) near(27?–28?S, 100?W) in September. The relative importance of horizontal density advection in determining the maximum ML location is discussed qualitatively. Downward Ekman pumping is key to determining the eastern boundary of the deep ML region. In addition, zonal density advection by the subtropical countercurrent(STCC) in the subtropical Southwest Pacific determines its western boundary, by carrying lighter water to strengthen the stratification and form a "shallow tongue" of ML depth to block the westward extension of the deep ML in the STCC region. The temperature advection by the STCC is the main source for large heat loss from the subtropical Southwest Pacific. Finally, the combined effect of net surface heat flux and meridional density advection by the subtropical gyre determines the northern and southern boundaries of the deep ML region: the ocean heat loss at the surface gradually increases from 22?S to 35?S, while the meridional density advection by the subtropical gyre strengthens the stratification south of the maximum ML depth and weakens the stratification to the north. The freshwater flux contribution to deepening the ML during austral winter is limited. The results are useful for understanding the role of ocean dynamics in the ML formation in the subtropical Southeast Pacific.     

西双版纳热带季节雨林树冠上生态边界层大气稳定度时间变化特征初探

为探讨热带季节雨林林冠上方大气稳定状态,为通量计算提供依据,利用2003-2004年热带季节雨林林冠上方的涡度相关法观测资料,对西双版纳热带季节雨林树冠上生态边界层内大气的稳定度频率分布进行了分析研究。计算了稳定度参数（z/L）,并对大气稳定度类型进行了划分,分析了大气稳定状态的时间变化。结果表明：在热带季节雨林林冠上方的大气稳定度频率分布存在明显的日变化。昼间不稳定状态占优势,晚上以稳定状态为主;在早晨和下午稳定状态和不稳定状态频率分布易发生变化,导致中性的大气稳定状态更容易出现;而各大气稳定状态的频率分布年和季节变化相对较小,大气不稳定状态出现频率以雾凉季最高、干热季最低;稳定状态出现频率以干热季最高、雨季最低;中性状态出现频率以雨季最高、雾凉季最低。