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文章信息
- 文华国, 罗连超, 罗晓彤, 游雅贤, 杜磊
- WEN HuaGuo, LUO LianChao, LUO XiaoTong, YOU YaXian, DU Lei
- 陆地热泉钙华研究进展与展望
- Advances and Prospects of Terrestrial Thermal Spring Travertine Research
- 沉积学报, 2019, 37(6): 1162-1180
- ACTA SEDIMENTOLOGICA SINCA, 2019, 37(6): 1162-1180
- 10.14027/j.issn.1000-0550.2019.066
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文章历史
- 收稿日期:2019-03-21
- 收修改稿日期: 2019-06-24
2. 成都理工大学沉积地质研究院, 成都 610059
2. Institute of Sedimentary Geology, Chengdu University of Technology, Chengdu 610059, China
区别于形成于流出地表的高温、近中性、氯碱性流体中的硅华/硅质沉积物[1-3],钙华是从泉水中经过有机和无机过程沉淀形成的淡水碳酸盐沉积物或碳酸盐岩[4],其沉积流体包括常温流体和热流体。近年来,虽然越来越多的学者倾向于使用“travertine”表示陆地环境下与热流体相关的碳酸盐沉积[5-9],但关于钙华名称的限定,尤其是“tufa”和“travertine”名称的选取,似乎不能明确钙华形成温度、外形、沉积环境等限定条件,可能无法准确表达复杂钙华类型完整的概念,如中国的四川黄龙沟钙华与云南白水台钙华,地球化学特征显示为热成因钙华(thermogene travertine)[10-12],若按照泉水温度的分类,四川黄龙沟钙华(约7 ℃)[13]与云南白水台钙华(约10 ℃)[14]属于冷水钙华(tufa)。基于此,本文对热泉钙华(thermal spring travertine)的定义为:沉淀于富Ca2+和HCO3-热泉(T≥20 ℃,普遍T≥30 ℃)[15]的陆地碳酸盐沉积物/岩。
目前,热泉钙华在古气候、古环境重建和油气勘探中扮演着越来越重要的角色,并引起国际上相关学者的关注。尽管相关学者对热泉钙华开展了相关研究:如热泉钙华与新构造运动的关系[16-19],热泉钙华的沉积格架与古环境重建[20-24],微生物在钙华形成中的作用[8, 25-28],钙华中特殊组构(如“方解石树”)的成因[29-32],热泉钙华的古气候重建[24, 33-35]等,但仍然存在一系列科学问题有待探索和研究。本文在阅读国内外大量文献的基础上,结合研究团队对云南腾冲热泉钙华的研究,阐述了热泉钙华的研究现状,包括热泉钙华时空分布、沉积特征、矿物组成、地球化学特征、微生物作用、流体来源、早期成岩作用、古气候记录等方面,并总结了热泉钙华研究意义,提出了当前热泉钙华研究存在的问题及下一步研究方向。
1 热泉钙华分类与时空分布目前,世界上针对钙华(travertine、tufa、calcareous tufa)的分类方式众多,常见的有成因分类、形态分类、温度分类等,如Pentecost et al.[36]按照CO2来源,将钙华分为大气成因钙华(meteogene travertine,δ13C多介于0~-11‰)与热成因钙华(thermogene travertine,δ13C介于-4‰ ~ 8‰),根据钙华体形态与发育位置将钙华分为原地钙华(autochthonous travertine)和碎屑钙华(clastic travertines)两个亚类,并进一步划分出了泉华丘、裂脊钙华和瀑布钙华等9个小类。Ford et al.[37]依据温度与发育位置将钙华分为冷水钙华(tufa)、热水钙华(travertine)和洞穴沉积物(speleothem)。热泉钙华属于热成因钙华或热水钙华,主要分布在第四纪,第四纪前的热泉古钙华发现较少,其原因可能是:1)热泉古钙华体规模较小和空间区域分布范围小,2)强烈的成岩改造,3)纹层状钙华与湖/海相叠层石的相似性导致的误判。
目前已发现/证实的热泉钙华主要分布于北半球,以第四纪和现代钙华发育为主(图 1),其具体时空分布特征表现为:
(1)受地热活动控制的现代热泉钙华报道最为丰富,如:中国云南腾冲地热区[31, 75-76]与西藏地区[77-78]、美国Yellowstone National Park[55, 79-80]、日本Nagano-yu Hot Spring[81]、冰岛Lýsuhóll地区[29, 82]、西班牙Alhama-Jaraba地区[83]。
(2)热泉活动已经停止的第四纪钙华也有较多发现,主要有:中国云南腾冲地区[30, 84-85]与西藏地区[35, 86-89]、加拿大Miette Hot Springs地区全新世残余钙华[45]与Fairmont Hot Springs地区的全新世钙华裙、意大利Tiber峡谷更新世瀑布钙华[24]与Euganean地热区更新世钙华丘[90]、土耳其Cakmak地区更新世钙华斜坡[80]。
(3)前第四纪热泉古钙华仅见于少数地区,研究程度较低,如匈牙利Budakalász的古近系钙华[66]、阿根廷Deseado Massif的侏罗纪地热区[56, 91-92]、欧洲Pechenga Greenstone Belt的古元古代钙华[20, 44]。在中国新疆柯坪硫磺沟地区也见有奥陶系古钙华出露[93-94],但是否为古热泉钙华还有待考证。
2 热泉钙华的沉积特征 2.1 沉积特殊性作为非海相碳酸盐岩的特殊沉积类型,区别于常见的湖相碳酸盐岩与石笋等洞穴沉积物,热泉钙华的沉积具有独特性,主要表现为:
(1)外形的多样性,表现为瀑布状、台地状、斜坡状、裂脊状、塔状、丘状等多种外形[76, 95-100](图 2)。
(2)沉积体系的多样性,可划分为斜坡沉积体系、凹陷沉积体系和Reed丘沉积体系(低角度斜坡沉积体系)[102],各类沉积体系下又分多个沉积相类型[52, 103]。
(3)岩相划分类型众多,可分为非生物结晶岩相、微生物岩相和碎屑颗粒岩相三大类,再细分为22个微相[103]。
(4)快速的相变,由于热泉水从泉口流向周缘过程中,温度急剧下降,热泉钙华沉积会很快过渡为冷水钙华(T < 20 ℃)[52]。
(5)沉积速率快[15],平均沉积速率可高达1.75 mm/年与30.9 mg/cm2/天[58, 104]。
(6)根据热泉喷口到远端裙距离和温度差异,可将热泉钙华沉淀环境划分为四类:喷口区、邻近斜坡、中裙和远端裙—沼泽[56](图 3、表 1)。
相组合 | 相 | 结构 | 叠层石组合 | 阿根廷Claudia | 阿根廷 Cerro Negro |
阿根廷 El Macanudo |
|
近端 | 喷口 | 水道/喉道 | √ | √ | |||
角砾 | √ | √ | |||||
沟渠 | √ | √ | |||||
针状/结节状/葡萄状 | 表层生物膜 | √ | |||||
串珠状 | |||||||
辐射微葡萄状 | √ | ||||||
近端斜坡 | 细层 | 表面生物膜 | |||||
水下 | 火山状锥 | 水道周围倾斜沉积 | 围绕水道基部呈花菜状 | √ | |||
同心锥 | 齿状同心层 | 微生物结构为主 | √ | ||||
管状 | 早期辐射柱状 | 管状物上的“花菜”包壳 | |||||
土丘/阶地 | 同心葡萄状/层状 | 结构中包含微生物 | √ | √ | |||
中端 | 流道 | 泡沫席 | 微生物结构为主 | √ | √ | ||
充填碎屑 | 暖流底部藻席(搬运) | √ | √ | ||||
带状结构 | 微生物结构为主 | √ | |||||
中裙池 | 厚栅状层 | 微生物结构为主 | √ | ||||
网状结构/锥形簇 | 微生物结构为主 | √ | √ | ||||
泡沫状结构 | √ | √ | |||||
远端 | 远裙 | 阶形/薄栅状层 | 微生物结构为主 | √ | √ | ||
低振幅波状层 | 生物+物理结构 | √ | √ | √ | |||
球晶/核形石 | 基本微生物结构 | √ | √ | ||||
沼泽 | 窗形 | 普遍在微生物沉积物形成 | √ | ||||
斑点状/凝结状/球状粒 | 微生物结构为主 | ||||||
植物/动物 | 某些地方,微生物岩包裹 | √ | √ | ||||
古土壤 | 风化硅华碎片,含微生物 |
第四纪热泉钙华的矿物组成主要包括非晶质碳酸钙、文石和方解石[105](图 4),尤以文石和方解石最为普遍[64, 108-109],而沉淀的非晶质碳酸钙由于不稳定,会快速转化为方解石和/或文石[110-112],这些关注和报道都相对较少[48]。钙华中矿物组成与温度、Mg/Ca比值、热液成分、CO2放气幅度、黏度、微生物、沉淀速率具有密切联系[38, 79, 113-116],但任何单一的控制因素都无法适用于任何地区。如腾冲热水塘地区与热海地区古钙华形成温度接近沸点[30, 76],根据Folk [114]的观点如此高温下形成的钙华应主要由文石组成,但事实却是热水塘地区与热海地区古钙华主要由方解石组成。同样的由方解石组成的高温钙华在肯尼亚Lake Bogoria[117-119]和新西兰[39]都有发现。因此,钙华的矿物组成是多因素综合作用的结果。此外,在部分热泉钙华中也发现了硫酸盐[120-121]和自生SiO2沉淀[122-123]的踪迹(图 4),这可能是由于热液原始组成与形成条件的差异等造成的。受控于热泉喷流活动的影响,也会存在或多或少的外源碎屑矿物[51];而成岩作用的改造也会导致钙华体中出现其他矿物,如白云石[51],且这种现象在越古老的钙华体中更为明显[20]。
3 热泉钙华的地球化学特征热泉钙华的地球化学特征更多的反映了热泉钙华形成主要受深源物质的加入与高温热流体的影响。与深部岩浆活动和/或深大断裂相关的热泉钙华由于受深源物质的混入影响,主要表现为:1)代表深循环流体的低U含量[124]与代表长期水岩反应的高234U/238U比值[125];2)热水沉积岩中常见的Eu正异常[7];3)深部来源Sr与其他来源Sr的混合[126];4)表示深源CO2混入的较高的δ13C值[127-128]。
形成热泉钙华的高温热流体地球化学性质可能表现为:1)低pH值、更高络合配位体浓度和/或表示更高温条件的高ΣREE值[7];2)较高的As与Te含量[123];3)高Mn与Fe含量[99, 129];4)较高的(普遍 > 50 ℃)流体包裹体均一化温度[47, 130-131];5)较高的氧同位素测温结果[85, 132]。
4 热泉钙华的微生物组成与意义生物在热泉钙华沉积中较常见[133-135],且在热泉钙华的识别与形成中意义重大。热泉的特殊环境条件决定了其内部生长的生物独特性(图 5)。在相对高温条件下,微生物主要以硫细菌与嗜热型微生物存在[8],如肯尼亚与新西兰的高温热泉(> 90 ℃)沉积物中广泛存在的嗜热型细菌[39]。随着水温与硫化物浓度的降低,温度对蓝细菌生长的抑制作用越趋变小[137],在水温低于50 ℃的环境下,丝状蓝绿藻在微生物中占据主导地位[6, 62]。
生物在热泉钙华的识别与形成中的意义包括三点:
(1)大型植物缺乏是热泉钙华区别于冷水钙华的重要标志[15],高温条件并不利于大型植物的生长,但对微生物活动限制弱[26, 82, 138-140],但是单一的植物证据并不能完全区分热水和冷水钙华,如热泉钙华内的树叶化石也可能源于周围高山上的植被[136]。
(2)微生物的发育一定程度上不利于钙华的沉淀,蓝细菌分泌的酸性物质或络合物(如胞外聚合物)会诱导小晶体的产生,而这类小晶体极有可能被溶解[141]。
(3)微生物对钙华的沉淀过程影响较大,蓝细菌的光合作用以及其他细菌的氨化作用、反硝化作用和硫酸盐还原作用能够诱导方解石或文石沉淀[142-143]。
5 热泉钙华的流体来源热成因钙华水来源对解释热泉钙华的成因机制[21, 144],区域构造断裂活动[22, 90],以及古环境和古气候重建[11, 22, 35, 37, 78, 145]等具有重要作用。形成热泉水的来源主要为大气降水,包括雨水、地表水、地下水,它们沿断层和断裂带渗入地下,与深循环水汇合,吸收热源热量,携带深源CO2向上输送到地表[146](图 6)。热泉钙华流体来源强烈受地热深部高二氧化碳流体的影响[9, 24, 99],主要体现在富CO2流体对渗入的大气水的贡献[24]。大部分热泉钙华是大气降水于构造活动区渗透于地下深部岩浆层携带深源CO2在地表脱气而成[147],如我国青藏高原[89, 148]、云南[144, 149-150]等构造地热活动强烈区,中非喀麦隆火山线[151],美国黄石公园[152-153]和伊朗北部Kopet-Dagh Zone[154]等。Karaisaoğlu et al.[109]认为Kavakköy钙华中高δ13C值和计算δ13C值与CO2来自于幔源有关。另外,基于氢氧同位素稳定化学性质和对水的标记作用,利用氢氧稳定同位素组成数据可区分泉水是否为大气降水补给来源[149]。位于永久冻土带的Pymvashor亚北极热液系统热泉流体δ18O和δ2H及其与大气降水H、O同位素组成的关系表明大气水在热液系统补给区域内的渗透[155]。同样,云南白水台温泉水δ2H、δ18O数据分布在大气降水线附近[144],也表明泉水的补给主要来源为大气降水;伊朗北部Ayub-Peighambar沉积钙华的热泉水δ2H、δ18O数据反映出泉水来源于沿深大断裂渗透的大气降水经过地下岩溶系统循环后经泉口排出[154]。
6 热泉钙华的早期成岩作用 6.1 热泉钙华的早期成岩作用定义及类型划分热泉钙华的早期成岩作用被定义为“发生或开始于沉积期或沉积期后的原始岩石组构的改变或转化过程”[156]。目前针对热泉钙华的早期成岩作用研究主要停留在早期成岩作用类型分析上[102, 157-161],系统性研究很少。由于早期成岩作用的过程发生很早,因此不管是正在活动的现代热泉钙华还是古钙华沉积都经历了一定程度的早期成岩作用改造,其早期成岩作用包括胶结作用、溶解作用、重结晶作用、交代作用、新生变形作用、泥晶化作用、角砾化作用、干缩裂缝、侵蚀作用、破裂作用、有机质腐烂、软沉积变形[52, 100, 102, 159, 162-164]。上述早期成岩作用中尤其是胶结作用、溶解作用、新生变形作用最为明显(图 7),其中胶结作用表现为:1)块状或板片状方解石[7, 136, 159];2)叶片状方解石等厚环边[164];3)他形方解石—文石壳、镶嵌状胶结物和增生胶结物[103, 136, 164]。陆地环境决定了热泉钙华受大气淡水的溶解作用明显,导致原生空隙的扩大、溶蚀空隙的产生和原生构造的破坏[159]。新生变形作用则主要表现为纤维状和泥晶状的文石向他形镶嵌状方解石晶体的转化[79, 159]。此外,泥晶化作用(图 7e)的出现也具有较大意义,可在一定程度上反映早期成岩过程微生物的活跃性[66, 100, 102]。
6.2 热泉钙华的早期成岩流体热泉钙华早期成岩流体的研究极少有报道。El Desouky et al. [165]利用流体包裹体与同位素地球化学手段对土耳其Denizli盆地的热泉钙华胶结物进行研究,发现其成岩流体为高温高盐度的流体。直观来看,陆相碳酸盐岩的早期成岩流体基本都是沉积物同期赋存流体与大气水,但这种认识并不完全适用于火山地热区热泉钙华的成岩流体判别,因为这些地区的热泉钙华受深部岩浆活动的影响较大,深部来源流体在其早期成岩过程中仍然十分重要,周期性的热泉活动带入的热流体很可能导致已固结钙华的早期成岩流体性质发生极大变化,这也使得其早期成岩流体中记录了热泉活动、深部流体来源强度等信息。
6.3 热泉钙华的早期成岩作用与微生物保存成岩作用会导致泉华沉积物中赋存的微生物或胞外聚合物信息的快速丢失[105]。Love et al. [166]认为纹层状钙华的新生变形作用会导致富生物纹层向柱状粗晶的转化,并最终丢失生物信息。Okumura et al. [62]在研究日本Nagano-yu Hot Spring钙华纹层时,发现蓝细菌生物膜会在10天内快速降解,留下类似于古叠层石的纹层状碳酸盐沉积物。这种生物痕迹丢失的现象在越古老的钙华中越明显[29, 85],如在俄罗斯Pechenga绿岩带中的前寒武系热泉钙华中微生物的痕迹已基本消失[20, 44]。这就带来了两个值得思考的难题:1)在古老热泉钙华中微生物的缺少到底是成岩作用还是沉积作用的结果,或者是沉积—成岩作用共同结果;2)如何才能从地质历史时期广泛发育的叠层石中识别出热泉钙华成因的叠层石。热泉钙华所处的陆地环境决定了其早期成岩作用必然会对其进行强烈改造,但如何改造及改造程度如何却依然是个值得深入研究的课题。
7 热泉钙华赋存的古气候记录信息及成岩作用对其的影响近期的研究[41, 167-168]表明,热泉钙华的形成会受到气候因素的控制,这种气候控制的特征体现为热泉钙华主要发育于温暖潮湿的间冰期,如中安第斯山更新世热泉钙华主要形成于MIS 3期与MIS 6期的间冰期潮湿气候条件[130]。Rihs et al. [43]认为,在湿润气候时期,大量的大气降水促进了热水系统循环和地下水位的增高,使得更多的热水运移排出在地表,从而有利于热泉钙华的形成,而在干旱寒冷期则相反。这些实例反映了热泉钙华气候记录信息能有效的重建古气候。但也有研究认为,气候对热泉钙华的形成影响较小,如土耳其Denizli Basin的更新世热泉钙华在干燥寒冷的MIS 2期也有发育[132]。显然,温暖潮湿的间冰期虽然有利于热泉钙华的形成[169],但并不意味着热泉钙华仅形成于温暖潮湿的间冰期。
关于古今热泉钙华与古气候记录关系的研究还多停留在用热泉钙华定年测定的形成时间与该时期的古气候记录对比上[24, 33-34, 87, 170](图 8),这种简单的对比是无法获得准确的古气候信息的,因为构造活动(如断层的开启与关闭)对钙华的形成也具有很大影响[17, 125, 170, 173]。因此,对赋存于热泉钙华中的古气候记录信息的提取,尤其是冷暖记录与降雨量记录信息的提取十分重要。
目前针对热泉钙华古气候记录的地球化学信息研究很少[63, 78, 174-175],这些研究明确了热泉钙华的碳、氧同位素与微量元素指标能较好的反映古气候信息(图 9)。如高竞[174]、覃建勋等[78]在U系法定年的基础上,参照古里雅冰芯δ18O的气候记录,对西藏荣玛钙华微量元素、稀土元素、氧同位素与古气候关系进行系统分析,进而挖掘钙华的古气候信息。研究发现,氧同位素在研究气候冷暖上更显优势[63, 173],而微量元素则与降雨量的关系密切[78]。需要注意的是,热泉钙华中的古气候信息的替代指标往往受到多因素的影响,如氧同位素组成除了受沉积期流体氧同位素组成和流体温度的影响[99, 167, 176],还受到成岩作用的改造;而微量元素的组成除了受到沉积流体成分等的影响外,也受到成岩作用的改造。
陆相碳酸盐岩成岩作用对地球化学信息的影响研究集中于洞穴沉积物[177-181]与冷水钙华[182-183]。由于早期成岩过程中不同期次的成岩胶结物、不同的有机组分或生物碎屑等的存在,许多类型的陆相碳酸盐岩都是非均匀相[156],使得其微量元素组成与氧同位素组成在经历早期成岩作用后都经历了不同程度的改变。例如,早期成岩作用导致中国神龙洞石笋的氧同位素变化了约0.85‰ [184],导致摩洛哥石笋的微量元素(Sr、Mg、Ba等)发生了不同程度的变化[185],导致Belgium地区冷水钙华的碳、氧同位素值不同程度的增加(其中δ13C增加约1.5‰[182])。这种发生在早期成岩过程中的地球化学特征的改变程度的研究十分薄弱[66, 158],而且部分研究并没有考虑成岩作用对同位素地球化学信息的影响[19, 24, 68, 165]。针对热泉钙华,这种早期成岩作用的过程发生很早,其对热泉钙华原生矿物改造和次生矿物形成的影响显著[156],继而影响并改变了反映古气候记录的地球化学信息。这种地球化学信息的微小改变往往对古气候分析具有重大影响。例如:土耳其Kocaba地区更新世热泉钙华在任何一个剖面上氧同位素变化值都不超过4‰[175],如果以早期成岩作用对洞穴沉积物氧同位素的改变值(0.85‰ ± 0.29‰)为参考标准[184],那么这种接近1‰的改变很可能导致古气候分析不准确,甚至获得完全相反的信息。因此,如果将这些受成岩改造可能发生改变或部分发生改变的古气候记录替代指标的直接应用,势必导致古气候意义解释的偏差,且这种认识及相关研究还未被重视。
8 研究意义及展望 8.1 研究意义(1)热泉钙华在中低纬度的火山地热区较发育,不严格受区域内碳酸盐岩地层展布的控制,且保存年龄较长,目前的研究已表明热泉钙华在古气候重建中的潜力[63, 78, 175],但其古气候替代指标却受到流体组成、沉积作用与环境因素、成岩作用的影响。有必要研究控制热泉钙华古气候替代指标的影响因素,并进行区域性和全球性气候类比,来评价热泉钙华在古气候重建中的意义及其实用性,为中低纬度地热区和碳酸盐岩贫乏区热泉钙华的古气候重建提供新启示。
(2)热泉地区的极端环境很可能是地球早期生物或者地外生物的生长环境[2, 55, 186],热泉钙华将可能成为揭示地球早期生命起源的钥匙之一。
(3)热泉钙华的发育与新构造运动的关系密切,是良好的构造运动指示工具[101, 187-188]。
(4)热泉钙华沉积可以作为人工CO2储库中CO2流失的研究代替物[68, 189-191]。
(5)目前针对非海相碳酸盐岩成岩机理的研究则主要集中在湖相碳酸盐岩,热泉钙华作为一种与岩浆和/或地热活动相关的非海相碳酸盐岩,通过研究其早期成岩作用机理,将增添非海相碳酸盐岩成岩作用研究新内容。
(6)近期在巴西Santos盆地和Campos盆地下白垩统[192-194]以及安哥拉Namibe盆地发现了油气勘探潜力巨大的储集层[195],热泉钙华在这些储层中占据了重要位置。另外,陆上地热资源在实际利用过程中存在严重的结垢问题,制约地热能高效利用,其结垢与热泉钙华沉淀具有极大相关性。因此,研究热泉钙华沉淀机理,对了解地热流体结垢机理及解决目前我国面临的化石能源短缺问题具有重要意义。
(7)与湖相热水沉积岩[196-200]在现代素材的稀缺与研究难度相比,热泉钙华具有更好的研究优势。热泉钙华作为常见的陆相热水沉积岩,在自然界广泛发育,这使得我们可以从现代热泉钙华出发,结合热泉古钙华研究,综合对比分析热泉钙华的地质地球化学特征,将进一步丰富和完善陆相热水沉积学理论。
8.2 存在的问题及下步展望近些年来,针对热泉钙华的研究呈现逐渐增多的趋势,岩石学、矿物学与碳氧同位素地球化学成为热泉钙华的必要研究手段,关于钙华成因、保存、微生物、沉积特征等的理解逐渐加深,但对热泉钙华的成因机制、与微生物作用关系、油气储集性评估、成岩作用机理和古气候重建等方面仍然存在很多问题亟待解决。
(1)热泉古钙华成因界定和时空演化不明确。钙华的古生物痕迹与碳氧同位素特征是划分大气成因钙华与热成因钙华、确定钙华形成古水温的主要手段;相比于现代热泉钙华,地质历史时期的热泉钙华缺乏热泉流体原始信息,无法获取热流体的氧同位素组成,无法计算获取沉积古水温,且由于经历了较强的成岩改造会进一步改变钙华原始碳氧同位素记录;另外,热泉古钙华缺乏生物痕迹(尤其是志留纪前),导致无法直接利用古生物痕迹定性区别钙华沉积古温度;即便确定了热泉古钙华成因,由于缺乏针对热泉钙华(甚至热泉泉华)的高分辨率(毫米至厘米级)沉积学和微观地层学研究,导致热泉古钙华时空演化不清楚。基于上述原因使得热泉古钙华成因界定和时空演化研究具有挑战性。
(2)热泉钙华矿物晶体形态及其成因研究薄弱。热泉钙华主要由方解石与文石组成,但是受水温、CO2分压、pH、流速等多种因素的影响,这两类矿物的形态却多种多样,尤其是方解石,可分为树状晶(结晶树状晶、非结晶树状晶)、骸晶、片状晶等多种类型,但对这些矿物晶形的成因与单因素的具体影响却了解甚少。
(3)热泉钙华的储集性能评估研究有待加强。巴西Santos盆地等地区巨大的非海相碳酸盐岩(疑似钙华)油气储/产层的发现,显示了钙华的良好油气潜力。储层特征与储集潜力的评估与成藏组合的刻画是油气开发与利用的重要基础,但是目前却仅有少数研究针对钙华物性分析,基本不见发育于湖泊周缘的钙华和陆地热泉钙华储层特征分析、储集潜力的评估与成藏组合的刻画。
(4)纹层状热泉钙华的生物成因与非生物成因不清楚。不同于冷水钙华或海/湖相叠层石,热泉钙华形成的高温环境不利于大多数微生物的发育,在热泉钙华中既发现了富生物的纹层,也发现了众多缺乏微生物痕迹的大段热泉钙华沉积。目前的研究初步显示热泉钙华的纹层似乎受到流速、间歇性暴露、CO2分压等的影响,但微生物在纹层状热泉钙华形成中的作用和影响程度尚不明确。
(5)热泉钙华成岩作用及其在古气候重建中的意义研究十分薄弱。成岩作用对古气候记录的影响研究对地热区古气候的重建具有重要指导。但目前国际上相关学者关于热泉钙华成岩过程的研究基本处于成岩作用识别与描述阶段[71, 100, 164],很少涉及热泉钙华早期成岩作用与古气候记录关系研究。一般而言,早期成岩作用很可能会改变热泉钙华原始矿物组构,甚至影响其内部保存的古环境与古气候信息,成岩过程中热泉钙华地球化学特征的变化能更准确的恢复其原始地球化学记录,但这种发生在成岩过程中的地球化学特征的改变程度的研究却极少。
综上所述,随着科技进步带来的实验手段的革新,建议加强如下方面热泉钙华的研究:1)古钙华形成环境与成因的替代指标(如包裹体温度、微生物痕迹)的建立,并利用高分辨率沉积学和微观地层学揭示热泉钙华沉积动力学机制和控制因素;2)热泉矿物形态的控制因素及矿物形态与环境的耦合性分析;3)湖缘热泉钙华的储集性分析及其与邻近相带的时空组合模式建立;4)微生物与非生物因素对纹层状钙华形成的具体影响与划分识别;5)热泉钙华矿物学与地球化学特征在成岩作用过程中的变化及其影响因素分析;6)热泉钙华的古气候意义与实用性评价。
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