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1.
物探测井在地热开发中的应用 总被引：3，自引：0，他引：3
地热资源的开发利用愈来愈受到广泛的重视 ,本文阐述了物探测井在地热开发中的作用 ,并介绍了视电阻率、温度、套管磁测井等方法在地热开发中的应用。 相似文献
2.
北京地热资源评价方法与信息管理系统研究 总被引：3，自引：0，他引：3
本文以系统工程理论为基础，提出地热水系统和地热信息管理系统的概念，并以北京地热资源为例，阐述了地热水系统计算评价和建立地热信息管理系统的具体方法和步骤。 相似文献
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青海共和盆地东部的贵德次盆扎仓地区发育复合型高温地热资源,先后施工完成的ZR1井3000 m裂隙型热储测温151.34℃, ZR2井4600 m干热岩热储测温214℃,展现共和盆地良好的地热资源潜力。本文首次报道ZR2井全井常规与特殊测井数据,评价了扎仓沟花岗岩热储的孔隙度、体积密度、岩石生热率、岩石力学、地应力等关键参数,结果显示:ZR2井温测井显示4 092.8 m温度达到180℃, 4602 m深度井温214℃;利用电成像测井识别出两段裂缝集中发育带,分别为4210—4220m和4310—4320m,并对全孔段裂缝的产状进行了统计分析;利用井壁崩落和三井径法,计算该钻孔现今最大主应力方向为近南北向;共解释岩性破碎地层(疑似含水)21.4 m/2层,岩性较完整地层70.4 m/7层,岩性完整地层376.1 m/27层,高放射性地层7.6 m/2层。热储测井解释结果为系统评价热储和开发利用提供参考。 相似文献
5.
热测井是直接测量地下岩层温度场分布的手段。岩石的热参数主要包括热导率、比热、产热流、热流密度等。了解岩层热参数及其空间分布特点在地壳运动研究、地热勘探及工程等方面具有重要价值。具有连续及原位测量特点的测井资料可用于计算地下岩层的各种热参数。本文介绍了大陆科学钻探中的热测井,说明了用测井资料计算热导率、比热、产热率、热流密度等热参数的方法,简述了热测井和热参数在科学研究以及工程方面的一些应用。 相似文献
6.
北京城区地热田某地热井热水地球化学研究 总被引：2，自引：0，他引：2
地热的开采会引起热储压力的降低 ,从而引起热流场的改变。热储压力的降低可能导致温度较低的地下水的流入 ,也可能导致深部更高温度热流体的补充 ,从而引起地热流体化学特征的变化。地热流体中一些组分的浓度依赖于热流体温度的高低。不同温度的水发生混合会破坏地热系统的化学平衡 ,从而改变地热流体的化学成分。因此 ,地热流体的化学监测可以提供许多有关地热系统变化的宝贵信息。由于长期开采 ,北京城区地热田的压力明显下降 ,并引起了地热水化学成分的细微变化。根据 1984年以来一眼地热井的地热水化学监测资料 ,研究了地热水的化学成分、地球化学温标的变化规律以及地热活动的总体强度和水 /岩平衡矿物中的示温矿物的变化趋势 ,说明地热的开采既引起了地热田水补给的加强 ,又导致了地热田热补给的加强 相似文献
7.
通过试验研究,井温测井同其它水文测井方法一样,可以确定被钻孔揭穿的含水层位置、厚度和钻孔中各含水层之间的水力联系;确定涌水层位置;确定漏水层位置;更主要的是可以解决一般水文测井方法难于解决的问题——有套管的井段和泥浆孔的含水层位置及其各含水层之间的水力联系。因此,对于富水性强,孔内不安全的钻孔可以采取先下套管,再做井温测量。若在一个地区或矿区曾系统做过井温测量,则用井温资料可以进行钻孔或剖面的含水层对比。下面着重介绍井温测井在水文地质及工程地质中的一些应用实例。 相似文献
8.
地热能作为可再生新型能源,其勘查开发利用具有高风险高投资的特点,因此,地热产业的发展需要国家政策的支持。本文在介绍了我国地热产业现状和政策的基础上,提出完善我国地热能产业开发利用政策的建议,以推动地热产业的良好发展,促进我国节能减排目标的顺利实现。 相似文献
9.
从潘塘断陷盆地地质、构造及水文地质条件等方面论证了形成地热必具的“源、通、储、盖”等要素，并与成热类型相似的北京“顺义－城区－良乡”地热带进行对比，认为潘塘断陷盆地存在较佳的地热储热条件。 相似文献
10.
地热为北京2008奥运会作贡献--2002北京地热国际研讨会综述 总被引：1，自引：0，他引：1
郑克掞 《水文地质工程地质》2003,30(2):109-109,19
以“地热与北京2008奥运会”为主题的北京地热国际研讨会于2002年10月29～31日在京召开,并取得圆满成功。会议由北京市国土资源与房屋管理局和北京市地质矿产勘查开发局主办。会议得到了国内外地热同行的积极响应,来自14个国家的22位专家和国内近200位代表出席了大会。其中包括国际地热协会主席意大利的Ｇ·卡佩蒂、国际地热协会副主席瑞士的Ｌ·赖贝奇、美国地热资源委员会主席Ｊ·伦德、联合国大学冰岛地热培训中心的Ｉ·弗里得莱夫森和新西兰奥克兰大学地热学院前院长Ｍ·零克斯坦,以及来自俄罗斯、匈牙利、波兰、保加利亚、捷克、斯… 相似文献
11.
We have applied the method of one temperature log suggested by Kutasov in 1987 to process an unsteady temperature log of the 674 m deep submarine borehole BDP-98-2 (Akademichesky Ridge, Lake Baikal) and found it suitable to reconstruct the primary steady thermal gradient not disturbed by drilling. The steady gradient we derived using a special formalism, with reference to drilling conditions and measured thermal properties of sediments, was 63 mK/m, more than two times the unsteady gradient at different depths. Heat flow calculated with this gradient and a mean thermal conductivity of 1.1 W/(m·K) was 70 mW/m2, which is consistent with earlier geothermal data from the same area. Thus, the one-log procedure is a useful tool to predict the original undisturbed thermal gradients and estimate approximate heat flows if a single unsteady temperature log is available. 相似文献
12.
T. M. Rachkovskaya 《Astronomy Reports》2003,47(10):865-872
We have studied the star 30 LMi using high-dispersion CCD spectra and photographic observations. We estimate the star's effective temperature Teff=7210 K, gravity log g=3.34, and microturbulence velocity ξt=5.8 km/s. The carbon abundance, log ?(C)=8.57, is close to the solar value. Nitrogen (log ?(N)=7.81), oxygen (log ?(O)=8.76), and sulfur (log ?(S)=7.20) are slightly underabundant compared to the Sun, by ?0.16 dex, ?0.11 dex, and ?0.13 dex, respectively. A relatively large underabundance of ?0.27 dex was found for titanium (log ?(Ti)=4.75), whereas zinc shows an over-abundance by +0.21 dex (log ?(Zn)=4.81). Sodium (log ?(Na)=6.26), silicon (log ?(Si)=7.57), calcium (log ?(Ca)=6.38), chromium (log ?(Cr)=5.62), iron (log ?(Fe)=7.51), nickel (log ?(Ni)=6.34), and yttrium (log ?(Y)=2.34) exhibited abundances close to the solar values. We find no chemical anomalies characteristic of Am stars or δ Scuti stars in the spectrum of 30 LMi. 相似文献
13.
T. M. Rachkovskaya 《Astronomy Reports》2002,46(9):760-764
We have studied the giant 20 Peg using high-resolution spectra. We derive the star’s effective temperature, T eff=6970 K, gravity, logg=3.35, and microturbulence velocity from FeI lines, ξt=2.70 km/s, and from NiI lines, ξt=2.45 km/s. The abundances of carbon, log?(C)=8.78, nitrogen, log?(N)=8.28, and silicon, log?(Si)=7.85, are enhanced compared to the solar values by 0.23, 0.31, and 0.30 dex, respectively. The abundances of oxygen, log?(O)=8.83, sodium, log?(Na)=6.37, and sulfur, log?(S)=7.33, are nearly solar. Calcium and nickel show normal abundances, log?(Ca)=6.44 and log?(Ni)=6.32. Iron log?(Fe)=7.63 and yttrium log?(Y)=2.41 are only slightly overabundant compared to the solar values (by 0.13 and 0.17 dex). We find a rather large (0.95 dex) overabundance of barium log?(Ba)=3.08. 相似文献
14.
The Roosevelt Hot Springs Known Geothermal Resource Area (KGRA) is a Basin and Range-type geothermal resource, which is located in southwestern Utah. The integrated multicomponent geothermometry (IMG) approach is used to estimate the reservoir temperature at the Roosevelt Hot Springs KGRA. Geothermometric modeling results indicate the deep reservoir temperature is approximately 284.6°C. A conceptual model of the Roosevelt Hot Spring KGRA is provided through integrating the various pieces of exploration information, including the geological data, geothermometric results, temperature well log and field evidence. A two-dimensional cross-sectional model was thus built to quantitatively investigate the coupled thermal-hydraulic processes in the Roosevelt geothermal field. By matching the preproduction temperature log data of deep wells, parameters controlling flow and heat transport are identified. The method and model presented here may be useful for other geothermal fields with similar conditions. 相似文献
15.
Experiments have been carried out to determine the temperature, oxygen fugacity (fO2) and compositional dependence of the tracer diffusion coefficient (D) of calcium in olivine. These data constrain the diffusion coefficient over the temperature range 900 to 1500°C for the three principal crystallographic axes. Well constrained linear relationships between the reciprocal of the absolute temperature and log(D) exist at any given oxygen fugacity. There is a strong dependence of the diffusion coefficient on oxygen fugacity with D ∝ fO2(1/3). This makes a knowledge of the T-fO2 path followed by geological samples a prerequisite for modelling Ca diffusion in olivine. The best fitting preexponential factor (Do) and activation energy (E) to the Arrhenius equation log (D) = log [Do exp(−E/RT)] + 0.31Δ log fO2 for Ca diffusion in olivine at a given oxygen fugacity (fO2*) are given by:diffusion along [100]: log [Do (m2/s)] = −10.78 ± 0.43; E = 193 ± 11 kJ/moldiffusion along [010]: log [Do (m2/s)] = −10.46 ± 0.37; E = 201 ± 10 kJ/moldiffusion along [001]: log [Do (m2/s)] = −10.02 ± 0.29; E = 207 ± 8 kJ/molwhere Δ log fO2 = log[fO2*] − log[10−12] with fO2* in units of bars. There is no measurable compositional dependence of the diffusion coefficient between Fo83 and Fo92. Diffusion in Fo100 has a much higher activation energy than in Fe-bearing olivine and has a weaker fO2 dependence. 相似文献
16.
Demezhko Dmitry Gornostaeva Anastasia Majorowicz Jacek Šafanda Jan 《International Journal of Earth Sciences》2018,107(1):113-121
International Journal of Earth Sciences - Using a previously published temperature log of the 2363-m-deep borehole Hunt well (Alberta, Canada) and the results of its previous interpretation, the... 相似文献
17.
N. I. Strel’tsova 《Geology of Ore Deposits》2009,51(5):398-413
The results of thermodynamic modeling of equilibriums between Cu, Fe, and Zn sulfides and oxides pertaining to the Cu-Fe-Zn-S-O2 system in water and aqueous chloride solution are presented. The system comprises solid phases of constant composition: pyrite,
pyrrhotite, hematite, magnetite, wüstite, γ-iron, chalcocite, covellite, cuprite, native copper, chalcopyrite, and bornite,
as well as more than 100 ions, complexes, and molecules in an aqueous solution.
The GIBBS program with the UNITHERM thermodynamic dataset used in calculations allows numerical analysis of phase assemblages
in a dry system and in equilibrium with an aqueous solution. How the temperature, pressure, and the composition of the solution
in the system opened for oxygen and sulfur affects the composition of phase assemblages was considered in temperature and
pressure ranges of 50–350 C and 100–1000 bar, respectively. Decrease in temperature leads to a shift in stability fields of
the studied phases toward the region of elevated oxygen and sulfur partial pressures. Variation of temperature is an important
factor affecting precipitation of ore minerals, primarily, Cu- and Zn-bearing. The calculation results are presented in tables
and diagrams. Each point in the $
(\log m_{S_{tot} } - \log f_{O_2 } )
$
(\log m_{S_{tot} } - \log f_{O_2 } )
diagram is characterized by a single possible assemblage of phases equilibrated with a solution of the given composition
within the considered temperature and pressure range. Since the composition of the mineral assemblage is controlled by physicochemical
conditions at the moment of mineral formation, comparison of the calculation results with mineral assemblages at ore deposits
makes it possible to estimate the parameters of ore deposition at the early stage of investigation, including oxygen and sulfur
activity and, occasionally, the composition and salinity of the solution. These parameters control the formation of such assemblages. 相似文献
18.
J. V. WALTHER 《Journal of Metamorphic Geology》1992,10(6):789-797
The equilibrium constant, K a , of the association reaction to form ion pairs from charged solute species in supercritical solutions can be calculated from a model based on published equations. Log K a at constant pressure is a linear function of the inverse in the dielectric constant of the fluid times temperature. The dielectric properties of H2 O and CO2 at supercritical pressures and temperatures can also be evaluated using the Kirkwood equation. Using Looyenga mixing rules, the dielectric constant of H2 O–CO2 mixtures can be obtained and the change in log K a with addition of CO2 in aqueous solutions evaluated. These changes in log K a with addition of CO2 are consistent with measured changes of log K a with addition of Ar in supercritical H2 O–Ar solutions.
Log Ka of KCl and NaCl increase to an increasing extent as the mole fraction of CO2 increases in H2 O–CO2 solutions. For instance, at 2 kbar and constant temperature between 400 and 600° C, log K a of KCl increases by about two orders of magnitude whilst that of NaCl increases by over four orders of magnitude as the CO2 mole fraction increases from 0.0 to 0.35. Such changes in log K a will have dramatic effects on the solubility of minerals in CO2 -rich environments. 相似文献
Log K
19.
W.F. Giggenbach 《Geochimica et cosmochimica acta》1982,46(12):2681-2683
The dominant process limiting CO2-contents of fluids in high temperature (>240°), liquid-dominated systems consists of the conversion of primary plagioclase by CO2 to calcite and clay according to log PCO2 = 15.26 ? 7850/(t + 273.2), temperature t in °C, with a likely error in log PCO2 due to variations in the activities of the anorthite and kaolinite components of the mineral phases involved of around ± 1 log unit. Secondary processes such as adiabatic expansion, conductive cooling and mixing with cooler groundwaters are largely responsible for subsequent variations in PCO2 at lower temperatures (>240°). 相似文献
20.
S.R Hart 《Geochimica et cosmochimica acta》1981,45(3):279-291
The temperature dependence of diffusion is usually found to follow the Arrhenius law: D = D0e?E/RT Winchell (1969) showed that there is commonly an inter-dependence between D0 and E (for diffusion in silicate glasses), such that diffusion of different species show a positive correlation on a log D0 vs E plot. A similar effect was noted by Hofmann (1980) for cation diffusion in basalt. This implies that diffusion rates of different species tend to converge at a particular temperature; this effect is known as the ‘compensation effect’. I will show that this effect is also present for diffusion in feldspars and olivines. The equations for the compensation lines (with E given in kcal/mol) are: basalt—E = 50 + 7.5 log D0 feldspar—E = 50.7 + 3.4 log D0 olivine—E = 78.0 + 7.5 log D0 The convergence, or crossover, temperatures for diffusion in various materials are: obsidian—3400°C basalt—1370°C olivine—1360°C feldspar—460°C Compensation plots are useful for evaluating and comparing experimental diffusion data (though of limited usefulness in a predictive sense) and for understanding ‘closure temperatures’ for diffusion in petrogenetic processes (since closure temperature, the temperature at which natural diffusion processes are frozen in, is dependent on E, log d0, and cooling rate). I show that most diffusing species in feldspar have a closure-temperature close to the crossover or convergence temperature, implying that all species in feldspars can be expected to ‘freeze-in’ simultaneously at temperatures in the range 400–600°C (for cooling rates in the range 101–105°C/myr). Closure temperatures of various species in olivine, on the other hand, span a much larger range (800°C) for a similar range in cooling rates, implying that different elements in olivine will record different time-temperature stages in petrogenetic processes. 相似文献