Variation Law of Mineral Emissivity Spectra with Mineral Granularity and Emission Angle Based on Hapke Model
-
摘要: 矿物红外发射光谱随粒度与发射角的变异是热红外地质遥感中的基础性问题之一, 温度与发射率反演以及矿物信息提取均需要考虑发射光谱的变异.常规实验室矿物发射光谱测量技术难度较大, 限制了对矿物发射光谱变异规律的深入研究.利用Hapke岩矿辐射传输模型对石英、白云母和钙长石3种矿物的发射光谱进行了模拟, 将模拟结果与实测光谱进行了对比, 总结了矿物发射光谱随粒度、发射角的变异规律, 分析了Hapke发射率模型存在的问题.Hapke模型可较好地模拟矿物发射光谱整体谱形与主要光谱特征及其变异规律, 但在某些光谱细节上与实测光谱仍有一定差异, 其原因可能是模型中矿物介质中多次散射辐射为“各向同性”的假设所致; 随粒度增加, 吸收特征会增强, 且位置可能发生漂移; 随发射角增加, 发射率逐渐减小, 透射特征和吸收特征逐渐增强, 但光谱的整体形状和透射特征、吸收特征、克里斯琴森特征的位置与形态均基本保持不变.Abstract: One of basic issues in thermal infrared remote sensing geology is the variation law of mineral emissivity spectra with mineral granularity and emission angle, and the law is required when several kinds of ground information are retrieved such as temperature, emissivity and mineral. However, the law is still unknown because it is difficult to measure the mineral emissivity spectra in the laboratory. In this experiment, emissivity spectra of quartz, muscovite and anorthite are calculated using Hapke radiative transfer model, and the calculation results are compared with measured spectra. Finally, the variation law of mineral emissivity spectra with granularity and emission angle is summarized, and the problem of Hapke emissivity model is analyzed. Research results show that, Hapke radiative transfer model could be used to simulate minerals emissivity spectral and variation, and some fine spectral features are different from measured spectral probably owing to Hapke model hypothesis in which multiscattering radiation is isotropic. The variation of spectral with granularity is complicated and the variation law is different to different minerals. The common law is that, with the increase of granularity, reststrahlen features strengthen, reststrahlen features and wavelength change, and Christensen features remain stable. With increase of emission angle, emssivity becomes lower, reststrahlen and transparency features become more obvious, and the whole spectral feature and wavelength of some features such as transparency, reststrahlen and Christensen features keep stable.
-
Key words:
- emissivity /
- mineral /
- infrared spectroscopy
-
江南隆起区处于扬子板块和华夏板块的结合部位(图 1), 是研究华南区域构造演化的关键地区.对区内的花岗岩体进行精确的年代学研究, 是建立华南构造-岩浆事件的年代学框架的关键.九岭位于江南隆起的中段(图 1), 九岭花岗岩体是我国华南的一个规模巨大的复式岩基, 对该岩体的系统研究将提供华南区域构造演化重要的信息.前人曾对该岩体进行了一些地质学、地质年代学的初步研究(江西省地质矿产局, 1984; 胡世玲等, 1985; 地矿部南岭项目花岗岩专题组, 1989; Li et al., 2003), 认为由晋宁、海西、燕山3个不同时代的花岗岩组成于新元古代形成的花岗岩统称九岭岩体.但不同人在不同地点取样、采用不同方法测年龄, 得出了不同的结果.对该复式岩基几乎没有做过系统的年龄测定, 因而未能建立起九岭地区花岗岩类形成的构造岩浆年代学骨架.此外, 华南新元古代花岗岩的成因是近几年研究的热点问题之一(徐夕生和周新民, 1992; Li, 1999; Li et al., 1999; Zhou et al., 2002; Li et al., 2003; Li et al., 2004; Wang et al., 2004; Zhou et al., 2004).过去认为加里东—海西花岗岩主要分布在华夏板块, 在扬子板块一侧也有少量产出(地矿部南岭项目花岗岩专题组, 1989), 然而扬子板块内部是否存在加里东—海西期的岩体尚须精确的年代学资料来证实.锆石SHRIMP年代学研究除了能精确测定花岗岩的成岩年龄外, 还可获得有关岩石成因方面的信息.本研究旨在厘定九岭复式花岗岩基的年龄框架, 为解决扬子地块东南缘花岗岩浆作用时代、花岗岩的物源等提供新信息.
图 1 九岭花岗岩地质简图及采样点位置Fig. 1. Sketch geological map of the Jiuling granitic complex and sampling sites1. 岩体地质概况
1.1 九岭岩体
九岭新元古代形成的花岗岩分布于江西省北部、九岭隆起带复式背斜的轴部, 呈近东西向至北东东向展布, 与区域构造线方向基本一致, 出露面积达2 500 km2, 为多次侵入的复式杂岩体, 过去统称为九岭岩体.九岭岩体是九岭复式花岗岩体的主体.该复式杂岩体已知有3次侵入: 第1次侵入的有九岭主体及黄岗口、仙源、白沙等岩体(江西省地质矿产局, 1984), 岩性主要为花岗闪长岩, 岩石呈灰-深灰色, 中-中粗粒结构、似斑状结构, 石英往往呈集合斑晶产出, 形成聚晶结构, 矿物成分为: 石英25%~30%, 钾长石5%~10%, 斜长石20%~40% (An10-42), 黑云母6%~13%, 堇青石1%~5%, 白云母2%~5%, 副矿物主要有锆石、磷灰石、石榴子石、钛铁矿等; 第2次侵入的有石花尖岩体, 岩石类型与第1次侵入的九岭岩体一致; 第3次侵入的有金钟湖、黄茅、南江、北坑等岩体, 主要由中细粒-细粒黑云母花岗岩、二云母花岗岩组成, 岩石呈浅灰色-微带肉红色, 花岗变晶结构, 少数具似斑状结构, 块状、片麻状构造, 与第1次、第2次花岗岩侵入体的区别是矿物颗粒较细, 钾长石含量较高.
九岭岩体与围岩接触关系基本上有2种: 侵入接触和混染交代接触, 局部地方见混合交代接触.岩体的北部、南东的一部分及东西两侧, 均明显侵入于中元古界双桥山群.在岩体北部罗溪镇一带, 下震旦统硐门组沉积于岩体之上(江西省地质矿产局, 1984).混染交代接触及混合交代接触主要出现在岩体南部, 岩体与围岩呈渐变关系, 形成类似混合片麻岩的接触带, 宽度一般为100~250 m.
胡世玲等(1985)用黑云母40Ar/Ar39快中子活化法测得937 Ma, 在高安县下观乡一带测得九岭岩体的黑云母K-Ar年龄为805 Ma (江西省地质矿产局, 1984)、838 Ma. Li et al. (2003)用锆石SHRIMP测得九岭岩体的U-Pb年龄为(819±9) Ma.
1.2 甘坊岩体
甘坊(上富) 岩体出露于上富—甘坊—潭山镇一带, 面积153 km2, 产于九岭隆起南侧, 呈北东向椭圆形(江西省地质矿产局, 1984).其主要岩性为灰白色粗粒黑云母或二云母花岗岩、花岗闪长岩, 部分岩石具似斑状结构, 斑晶为钾长石.与九岭岩体的岩性相比, 岩石色浅, 黑云母含量较低, 白云母含量较前者高, 矿物颗粒粗大, 含钾长石大斑晶, 在潭山镇一带, 岩石的风化物中有大量自形的高温石英的副像.在甘坊镇东北约14 km处, 可见灰白色粗粒二云母花岗岩与九岭岩体的中粒灰色-深灰色黑云母花岗闪长岩接触带, 二者呈截然接触, 但未见相互穿插关系.在奉新县上富镇西南面用白云母K-Ar法测得年龄值为257 Ma、204 Ma (江西省地质矿产局, 1984).
1.3 燕山期岩体
在古阳寨、甘坊镇东南面、九仙塘镇和修水县以南, 燕山期的岩体侵入于前期形成的岩体中.其中古阳寨岩体出露于宜丰、奉新两县交界处, 侵入于甘坊岩体中, 出露面积66 km2 (江西省地质矿产局, 1984).岩性主要为中细粒黑云母花岗岩, 此外还有中细粒二云母花岗闪长岩和少量的淡色花岗岩.九仙塘岩体侵入于晋宁期九岭岩体中, 岩性为中细粒黑云母花岗岩.在古阳寨北侧用黑云母K-Ar法测得岩体年龄值为177 Ma, 划分为燕山早期, 九仙塘岩体被认为是燕山中期的产物(江西省地质矿产局, 1984).
2. 锆石阴极发光(CL)、背散射(BSE)图像观察及U-Pb SHRIMP分析
2.1 样品描述及分析方法
在详细的野外工作、显微镜观察的基础上, 选择了代表晋宁期、海西期和燕山期的新鲜岩石样品来挑选锆石, 采样位置见图 1及表 1.每个样品破碎后过60目的筛, 经淘洗及电磁选分选出锆石, 并在双目显微镜下挑选出晶形较完好、纯净透明的颗粒用于测试.各期锆石的形态特征描述见表 1.
表 1 采样位置及锆石形态特征Table Supplementary Table Sampling positions and morphology of zircons
将待测的锆石与标样(TEM, 用于校正年龄, 其年龄为417 Ma) 一起用环氧树脂包埋制成圆形的靶, 然后把锆石抛光至一半.样品靶制好后先进行透射与反射光下的显微照相, 然后在北京地质矿床所先进行阴极发光(CL)和背散射(BSE) 照相, 以确定锆石颗粒的内部结构及适合分析的锆石颗粒与位置供SHRIMP测定.靶完成镀金后, 锆石的U、Th和Pb同位素组成分析在北京离子探针中心SHRIMP Ⅱ离子探针上进行. 详细的分析流程和原理参考文献Williams (1998)和万渝生等(2004).
应用SL13 (年龄572 Ma, 238U含量238 μg/g) 标定样品的U、Th含量.每分析一次标样TEM, 然后分析2~4个待测锆石点, 对锆石标样TEM的U/Pb比值分析偏差为0.5%~1.9% (1σ).采用年龄为206Pb/238U年龄(老锆石采用206Pb/207Pb年龄进行讨论), 其加权平均值为95%的置信度.年龄计算中, 普通铅校正采用204Pb直接测定法, 年龄置信度为1δ (95%置信水平).
2.2 分析结果
2.2.1 锆石阴极发光(CL)、背散射(BSE)图像
在阴极发光和背散射图像中, 各时期形成的锆石均具有清晰的振荡环带, 部分锆石中间具有核, 核部较圆, 透明度差, 边部具有环带的部分应为岩浆结晶形成的锆石, 中间的核为继承锆石.3个样品中, 九仙塘J07中的锆石不如九岭、甘坊岩体中锆石纯净, 含较多的包裹体, 并且也有继承核(图 2).
图 2 锆石阴极发光(CL)和背散射(BSE)图像圈和数字分别表示U-Pb分析点中心和206Pb/238U年龄Fig. 2. BSE and CL imagings of zircons2.2.2 锆石SHRIMP测定结果
(1) J39测试结果.对该样中17颗锆石进行了20次分析, 结果见表 2.其中的14次分析均在环带状岩浆锆石上进行, U的含量为(167~693) ×10-6, Th的含量为(30~183) ×10-6, Th/U比为0.09~0.68, U、Th含量变化较大, 它们在谐和线上构成一致的年龄组(图 3b), 其206Pb/238U加权平均年龄为(828±8) Ma (95%置信水平), 该年龄应代表岩体主体的形成年龄.这与Li et al. (2003)发表的年龄数据(819±9) Ma是非常接近的.
6.2、10.1和14.1分析点在形态自形的锆石的环带部位进行, 给出近一致的206Pb/238U年龄分别为(910±16) Ma、(881±16) Ma、(869±15) Ma.这3颗锆石可能是捕虏晶, 也可能是先形成的岩浆锆石.
6.1、8.1、11.1在锆石的核部上进行分析, 分别给出了(1 655±6) Ma、(1 459±11) Ma和(1 720±6) Ma近一致的Pb-Pb谐和年龄值(表 2).这些继承核毫无疑问是花岗岩形成过程中的熔融残余, 它们的Th/U比较高, 其年龄值为继承锆核形成的年龄.
表 2 九岭花岗岩J39号样的锆石SHRIMP U-Pb分析结果Table Supplementary Table SHRIMP U-Pb data of sample J39 of Jiuling granite
2. JX03-13分析结果
对该样品中的13颗锆石进行了13个点的U-Pb同位素年龄分析, 结果见表 3.所分析的锆石颗粒为透明的自形晶体, 阴极发光和背散射图像均显示岩浆结晶成分环带(图 2b).大多数分析点的U含量为(258~476) ×10-6, Th的含量为(40~387) ×10-3, Th/U大于0.1.除3个分析点的数据明显偏离变化范围外, 10个分析点的206Pb/238U一致年龄加权平均值为(820±10) Ma (图 4a).说明甘坊岩体形成于新元古代.这一结果与原来的研究结果有很大的差别.前人用白云母K-Ar法测出岩性为浅灰色粗粒二云母或含黑云母花岗岩的年龄为257 Ma, 从而单独划分出海西期的甘坊花岗岩体(江西省地质矿产局, 1984).由于这一测年方法不适于测定年龄较老的岩石, 因此所得年龄并不能代表花岗岩的形成年龄.
表 3 甘坊花岗岩JX03-13号和九仙塘花岗岩J07的SHRIMPU-Pb锆石年龄分析结果Table Supplementary Table SHRIMP U-Pb data of samples JX03-13 and J07 of Ganfang and Jiuxiantang granites
图 4 JX03-13和J07锆石SHRIMP U-Pb一致线图解Fig. 4. Zircon SHRIMP U-Pb concordia diagram of samples JX03-13 and J071.1的年龄值比其他锆石颗粒略大, 其可能的成因解释同J39中的分析点6.2、10.1和14.1;2.1、3.1的年龄值明显低于其他颗粒, 可能代表较晚结晶的锆石; 4.1的Th/U低(0.09), 体现出明显的Pb丢失, 年龄值明显老于其他锆石, 应为捕虏晶.
3. J07分析结果
对J07号样做了15颗锆石15个点的分析, 分析点全都打在锆石的环带部分, U的含量为(657~6 404) ×10-6, Th的含量为(393~1 832) ×10-6, U、Th含量都比较高, Th/U比为0.22~0.80, 给出了(140~167) Ma的206Pb/238U年龄值(表 3).由图 4b可看出, 绝大部分的锆石形成于150 Ma左右, 因此取数据分布集中区域的11个点加权平均得(151.4±2.4) Ma, 该年龄代表岩体的形成年龄.
本次测定结果与原来把九仙塘岩体划分为燕山中期的研究结果是一致的.
4. 讨论
九岭花岗岩基主要由~830 Ma的花岗岩组成, 也存在~150 Ma的花岗岩, 但不存在海西期花岗岩.过去认为华南扬子、华夏板块均存在加里东—海西期的岩体, 这一时期的岩体主要分布在华夏板块一侧, 扬子板块一侧有零星出露(如过去认为的湖南桃江、板杉铺、吴集、白马山、甘坊等); 而印支期的花岗岩在扬子陆块和华夏陆块内均有出露(地矿部南岭项目花岗岩专题组, 1989).本课题组对过去被认为是加里东期的湖南桃江岩体进行的锆石SHRIMP定年结果(续海金等, 2004) 表明该岩体形成于印支期, 本文研究的甘坊岩体也并非海西期产物, 由此推测扬子板块内可能不存在加里东期的岩体, 只是到了印支期, 扬子板块和华夏板块才具有统一的岩浆活动特征.晚元古代花岗岩中的残余锆石年龄集中在1.4~1.9 Ga, 这些继承锆石的Th/U比较高, 其年龄代表锆石结晶的年龄, 也可能代表九岭新元古代花岗岩源岩的年龄.
锆石的阴极发光照相、SHRIMP测试得到了北京地质矿床所和北京离子探针中心的帮助和支持, SHRIMP分析是在万渝生老师的精心指导下进行的, 在此一并表示衷心感谢! -
图 1 石英发射光谱特征(据Melissa and Christensen, 1996修改)
Fig. 1. Emissivity features of quartz
图 2 石英计算光谱与ASU光谱库中实测光谱的对比
Fig. 2. Comparison of calculated quartz emissivity and ASU emissivity
图 4 白云母计算光谱与ASU光谱库中实测光谱对比
Fig. 4. Comparison of calculated muscovite emissivity and ASU emissivity
图 5 计算的不同粒度白云母的发射光谱
Fig. 5. Calculated muscovite emissivity of different granularities
图 6 钙长石计算光谱与ASU光谱库中实测光谱对比
Fig. 6. Comparison of calculated anorthite emissivity and ASU spectral emissivity
图 7 计算的不同粒度钙长石的发射光谱
Fig. 7. Calculated anorthite emissivity of different granularities
表 1 石英的分散度参数
Table 1. Dispersion parameters of quartz
-
[1] Aronson, J. G., Strong, P. F., 1975. Optical constants of minerals and rocks. Applied Optics, 14 (12): 2914-2920. doi: 10.1364/AO.14.002914 [2] Bandfield, J. L., 2002. Global mineral distributions on Mars. Journal of Geophysical Research, 107 (E6): 5042-5063. doi: 10.1029/2001JE001510 [3] Bandfield, J. L., Hamilton, V. E., Christensen, P. R., 2000. A global view of Martian surface composition from MGS-TES. Science, 287 (5458): 1626-1630. doi: 10.1126/science.287.5458.1626 [4] Buratti, B. J., Hicks, M. D., Soderblom, L. A., et al., 2004. Deep space 1 photometry of the nucleus of Comet19P/Borrelly. Icarus, 167 (1): 16-29. doi: 10.1016/j.icarus.2003.05.002 [5] Christensen, P. R., Bandfield, J. L., Hamilton, V. E., et al., 2000. Athermal emission spectral library of rock-forming minerals. Journal of Geophysical Research, 105 (E4): 9735-9739. doi: 10.1029/1998JE000624 [6] Clark, R. N., Swayzer, G. A., Livo, K. E., et al., 2003. I maging spectroscopy: Earth and planetary remote sensing with the USGS Tetracorder and expert system. Journalof Geophysical Research, 108 (E2): 5131. [7] Conel, J. E., 1969. Infrared emissivities of silicates: Experimental results and a cloudy at mosphere model of spectral emission from condensed particulate mediums. Journal of Geophysical Research, 74 (6): 1614-1634. doi: 10.1029/JB074i006p01614 [8] Copper, B. L., Salisbury, J. W., Killen, R. M., et al., 2002. Midinfared spectral features of rocks and their powders. Journal of Geophysical Research, 107 (E4): 5017. doi: 10.1029/2000JE001462 [9] Cruikshank, D. P., Dalle-Ore, C. M., Roush, T. L., et al., 2001. Constraints on the composition of Trojan asteroid 624 Hector. Icarus, 153 (2): 348-360. doi: 10.1006/icar.2001.6703 [10] Dozier, J., Warren, S. G., 1982. Effect of viewing angle on infrared brightness temperature of snow. Water Resources Research, 18 (5): 1424-1434. doi: 10.1029/WR018i005p01424 [11] Hamilton, V. E., 2000. Thermal infrared emission spectroscopy of the pyroxene mineral series. Journal of Geo-physical Research, 105 (E4): 9701-9716. doi: 10.1029/1999JE001112 [12] Hansen, J. E., Travis, L. D., 1974. Light scattering in planetary at mospheres. Space Science Review, 16 (4): 527-610. doi: 10.1007/BF00168069 [13] Hapke, B., 1981. Bidirectional reflectance spectroscopy 1. Theory. Journal of Geophysical Research, 86 (B4): 3039-3054. doi: 10.1029/JB086iB04p03039 [14] Hapke, B., 1984. Bidirectional reflectance spectroscopy: 3. Correction for macroscopic roughness. Icarus, 59 (1): 41-59. doi: 10.1016/0019-1035(84)90054-X [15] Hapke, B., 1986. Bidirectional reflectance spectroscopy: 4. The extinction coefficient and the opposition effect. Icarus, 67 (2): 264-280. doi: 10.1016/0019-1035(86)90108-9 [16] Hapke, B., 1993a. Combined theory of reflectance and emit-tance spectroscopy. In: Remote geochemical analysis: Elemental and mineralogical composition. CambridgeUniversity Press, London, 31-41. [17] Hapke, B., 1993b. Theory of reflectance and emittance spectroscopy. Cambridge University Press, London. [18] Hapke, B., 1999. Scattering and diffraction of light by particles in planetary regoliths. Journal of Quantitative Spectroscopy of Radiative and Transfer, 61 (5): 565-581. doi: 10.1016/S0022-4073(98)00042-9 [19] Hapke, B., 2002. Bidirectional reflectance spectroscopy: 5. The coherent backscatter opposition effect and anisotropic scattering. Icarus, 157 (2): 523-534. doi: 10.1006/icar.2002.6853 [20] Hapke, B., Nelson, R., Smythe, W., 1998. The oppositio neffect of the moon: Coherent backscatter and shadow hiding. Icarus, 133 (1): 89-97. doi: 10.1006/icar.1998.5907 [21] Hudson, R. S., Ostro, S. J., 1999. Physical model of asteroid 1620 Geographos from radar and optical data. Icarus, 140 (2): 369-378. doi: 10.1006/icar.1999.6142 [22] Kahle, A. B., Alley, R. E., 1992. Separation of temperature and emittance in remotely sensed radiance measurements. Remote Sensing of Environment, 42 (2): 107-111. doi: 10.1016/0034-4257(92)90093-Y [23] Kirkland, L., Herr, K., Keim, E., et al., 2002. First use of an airborne thermal infrared hyperspectral scanner for compositional mapping. Remote Sensing of Environment, 80 (3): 447-459. doi: 10.1016/S0034-4257(01)00323-6 [24] Klingelh fer, G., Morris, R. V., Bernhardt, B., et al., 2004. Jarosite and hematite at Meridiani planum from opportunity's MÖssbauer spectrometer. Science, 306 (5702): 1740-1745. doi: 10.1126/science.1104653 [25] Lane, M. D., Christensen, P. R., 1997. Thermal infrared emission spectroscopy of anhydrous carbonates. Journal of Geophysical Research, 102 (E11): 25581-25592. doi: 10.1029/97JE02046 [26] Li, X. W., Wang, J. D., Strahler, A. H., 1999. Scale effects of Planck's law over nonisothermal blackbody surface. Science in China (Series E), 42 (6): 652-656. doi: 10.1007/BF02917003 [27] Liu, L. W., Zheng, H. B., Jian, Z. M., 2005. Visible reflectance record of South China Sea sediments during the past 220 ka and its implications for East Asian monsoon variation. Earth Science—Journal of China University of Geosciences, 30 (5): 543-549 (in Chinesewith English abstract). [28] Liu, Z. F., Christophe, C., Alain, T., 2005. Application of Fourier transform infrared (FTIR) spectroscopy in quantitative mineralogy of the South China Sea: Example of core MD01-2393. Earth Science—Journal of China University of Geosciences, 30 (1): 25-29 (inChinese with English abstract). [29] Mallama, A., Wand, D., Howard, R. A., 2002. Photometry of mecury from SOHU/LASCO and earth: The phase function from 2 to 170°. Icarus, 155 (2): 253-264. doi: 10.1006/icar.2001.6723 [30] McGuire, A. F., Hapke, B. W., 1995. An experimental study of light scattering by large, irregular particles. Icarus, 113 (1): 134-155. doi: 10.1006/icar.1995.1012 [31] Melissa, L. W., Christensen, P. R., 1996. Optical constants of minerals derived from emission spectroscopy: Application to quartz. Journal of Geophysical Research, 107 (B7): 15921-15931. [32] Moersch, J. E., Christensen, P. R., 1995. Thermal emission from particulate surfaces: A comparison of scattering models with measured spectra. Journal of GeophysicalResearch, 100 (E4): 7465-7477. [33] Pit man, K. M., Wolff, M. J., Clayton, G. C., 2005. Application of modern radiative transfer tools to model laboratory quartz emissivity. Journal of Geophysical Research, 110 (E08003): 1-15. [34] Poulet, F., Cuzzi, J. N., Cruikshank, D. P., et al., 2002. Comparison between the Shkuratov and Hapke scattering theories for solid planetary sufaces: Application to the surface composition of two Centaurs. Icarus, 160 (2): 313-324. doi: 10.1006/icar.2002.6970 [35] Reinart, A., Reinhold, M., 2008. Mapping surface temperature in large lakes with MODIS data. Remote Sensing of Environment, 112 (2): 603-611. doi: 10.1016/j.rse.2007.05.015 [36] Salisbury, J. W., Wald, A., 1992. The role of volume scattering in reducing spectral contrast of reststrahlen bands in spectra of powdered minerals. Icarus, 96 (1): 121-128. doi: 10.1016/0019-1035(92)90009-V [37] Salisbury, J. W., Walter, L. S., 1989. Thermal infrared (2.5-13.5μm) spectroscopic remote sensing of igneous rock types on particulate planetary surfaces. Journal of Geophysical Research, 94 (B7): 9192-9202. doi: 10.1029/JB094iB07p09192 [38] Shepard, M. K., Helfenstein, P., 2007. A test of the Hapke photometric model. Journal of Geophysical Research, 112 (E03001): 1-17. [39] Simonelli, D. P., Veverka, J., Thomas, P. C., et al., 1996. Ida lightcurves: Consistency with Galileo shape and photometric models. Icarus, 120 (1): 38-47. doi: 10.1006/icar.1996.0035 [40] Spitzer, W. G., Kleinman, D. A., 1961. Infrared lattice bands in quartz. Phsical Review, 121 (5): 1324-1335. doi: 10.1103/PhysRev.121.1324 [41] Vaughan, R. G., Calvin, W. M., Taranik, J. V., 2003. SE-BASS hyperspectral thermal infrared data: Surface emissivity measurement and mineral mapping. Remote Sensing of Environment, 85 (1): 48-63. doi: 10.1016/S0034-4257(02)00186-4 [42] Vaughan, R. G., Hook, S. J., Calvin, W. M., et al., 2005. Surface mineral mapping at streamboat springs, Neveda, USA with multi-wavelength thermal infrared images. Remote Sensing of Environment, 99 (1-2): 140-158. doi: 10.1016/j.rse.2005.04.030 [43] Wald, A. E., Salisbury, J. W., 1995. Thermal infrared directional emissivity of powdered quartz. Journal of Geophysical Research, 100 (B12): 24665-24675. doi: 10.1029/95JB02400 [44] 刘连文, 郑洪波, 翦知湣, 2005. 南海沉积物漫反射光谱反映的220ka以来东亚夏季风变迁. 地球科学———中国地质大学学报, 30 (5): 543-549. https://www.cnki.com.cn/Article/CJFDTOTAL-DQKX200505004.htm [45] 刘志飞, Christophe, C., Alain, T., 2005. 傅里叶变换红外光谱(FTIR) 方法在南海定量矿物学研究中的应用: 以MD01-2393孔为例. 地球科学———中国地质大学学报, 30 (1): 25-29. https://www.cnki.com.cn/Article/CJFDTOTAL-DQKX200501002.htm -
下载:
下载:
点击查看大图
计量
- 文章访问数: 3639
- HTML全文浏览量: 91
- PDF下载量: 83
- 被引次数: 0
