A REVIEW OF PALEOCLIMATIC CHANGES IN CHINA BASED ON PEAT CELLULOSE ISOTOPIC RECORDS
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摘要: 泥炭作为一类重要的地质载体,在开展古气候(尤其是全新世古气候)变化研究方面,具有一些其他地质载体所不具备的天然优势,特别适合开展有机地球化学和同位素地球化学方面的研究工作。概括了目前我国泥炭纤维素同位素研究的现状,对已经获得的数据进行了详细的总结和分析,结合与其他地质载体所获得的最新成果的对比,指明了目前我国泥炭纤维素同位素应用于古气候研究当中所存在的一些问题。产生这些问题的一个重要原因很可能是由于缺乏详细的现代过程研究,以至泥炭纤维素同位素代用指标的古气候指示意义因缺乏现代参照而不能加以明确。在此基础上,对我国泥炭纤维素同位素的进一步研究进行了展望,指出了在以后研究当中值得注意的几个方面。Abstract: Peat, as an important geological archive, has some internal advantages over other geological archives in researching paleoclimatic changes (especially the paleoclimatic changes during Holocene), and is particularly suitable for organic geochemistry and isotopic geochemistry studies. There are many peat bogs in China. Various researches have been conducted on these peat archives by both the domestic and international scientists,and important progresses have been reached. In this paper, we made a comprehensive review of the reported stable isotopic results for peat cellulose in China. The available data has been carefully collected and analyzed, upon the comparison with the latest results of paleoclimatic reconstruction obtained from other geological archives, then discussed are the critical problems about the application of peat cellulose isotopes in paleoclimatic research. We believe that these problems come from the insufficient study of modern-process. Therefore, the paleoclimatic significance of the stable isotopes of peat cellulose from a specific locality is not certain, due to lack of modern analogues. Finally, a discussion was devoted to the future development of stable isotopes of peat cellulose in China and some methodological problems.
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Keywords:
- peat /
- cellulose /
- carbon、oxygen isotope /
- palaeoclimate /
- modern-process study
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近年来，随着对深海环境的进一步勘探，在深水盆地边缘发现了许多重力流沉积的产物。人们通过对陆架、陆坡和盆地底部的高分辨率地震资料的分析将这些复杂的重力流沉积特征进行了详细研究[1]。其中块体搬运沉积（MTDs）是深水重力流沉积中的重要组成单元。MTDs是指由于滑动、滑塌、碎屑流等重力流沉积因素，顺着陆坡从高地移动到坡度较低地区的过程中所形成的沉积体[2-3]。前人的研究中，MTDs存在于许多深水盆地边缘地层中，甚至达到陆坡边缘盆地面积的50%，它还是深海沉积物输运的重要来源之一[4-5]。2016年对意大利Maiolica白垩纪碳酸盐岩的研究表明，该盆地地层中MTDs约占50%～60%[6]。由于块体搬运沉积广泛发育于浅海—深海中的陆架边缘盆地中，因此，对其深入研究有助于认识海底地形和构造活动，为深水领域油气资源勘探与预防海底地质灾害提供有利依据。
但是由于MTDs多发育于深海沉积环境中，我们无法直观地通过观察其外部特征与内部结构来识别，因此需要借助高分辨率的地震资料、回声探测、多波束测深系统等对其进行表征与识别[7-8]。本文基于琼东南盆地陵水凹陷高分辨率三维地震资料，发现在陵水凹陷陆坡处发育有大量重力流沉积的产物，其中块体搬运沉积占有较大比例。由于海底陆坡和盆地底部的沉积体系是以重力流沉积为主，因此MTDs的广泛发育会影响海底形态和MTDs之后地层的沉积与构造变形，还会影响水道的发育位置[3,9]。但现在的研究依然没有足够的证据表明MTDs内部构造的发育对上覆地层沉积的影响，以及它是如何影响和控制后期地层沉积的。本文基于以上问题，研究国内外最新成果，对本地区MTDs进行刻画和分析，重点研究MTDs内部构造特征和它对后续地层沉积的影响。
1. 地质概况
琼东南盆地位于中国海南岛南部，整个盆地面积约为4.5×104 km2，整个盆地呈NE方向展布[10]。陵水凹陷位于琼东南盆地深水区，西部与乐东凹陷相连位于琼东南盆地中央坳陷带，南部为陵南低凸起，北部与陵水-松南低凸起连接，东部为松南低凸起。研究区位于陵水凹陷陆坡区，是连接浅海陆架与深海平原的过渡区（图1）。陵水凹陷主要沉积的新生代地层包括始新统、渐新统崖城组和陵水组，中新统三亚组、眉山组和黄流组，上新统莺歌海组及第四系，新生代整体沉积的地层厚度约10 km[10-11]。陵水凹陷新生代地层主要经历了古近纪的裂陷期、新近纪和第四纪的裂后期，裂后期沉积又根据沉降速率划分为热沉降期和加速沉降期，共3大构造演化阶段。在加速沉降阶段的后期，整个琼东南盆地构造活动逐渐稳定，北部海南岛为盆地提供了充足的物源[10]。研究区内目的层段主要发育于第四纪，第四纪的沉积模式主要为陆架陆坡海相沉积，由于陆架边缘的物源供给充足，这些沉积物受重力流沉积作用，在沿陆坡向下不断推进沉积的过程中会发育块体搬运沉积体、水道和峡谷等[12-14]。
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图 1 琼东南盆地陵水凹陷位置与研究区MTDs1现今地貌图Figure 1. Location of Lingshui Sag, Qiongdongnan Basin and the MTDs1 current2. MTDs在地震资料上的识别
由于深水地区资料有限，目前深水MTDs的识别方法仍以地震资料为主，用有限的常规测井资料、岩心等数据辅助解释[15]。地震资料是目前识别深水MTDs最常见、最主要的方法。它主要是根据地震波对MTDs边界及内部运动的响应特征来判断MTDs的形态与搬运过程[8,15]。在地震上常见的陡崖、擦痕、杂乱反射、趾部的逆冲构造等识别标志可以判断MTDs的规模、搬运方向等（图2）[15]。利用地震属性资料，如均方根、瞬时频率、相干体、时间切片等，可以进一步识别MTDs的平面展布、内部特征等[2,15]。在常规的测井曲线上MTDs的特征通常为漏斗形和箱形的组合，顶界面为突变或渐变的接触关系，曲线主要为弱齿状或齿状[8,15-16]。在测井资料识别中，以地震资料解释为前提，用井-震结合的方法，对MTDs的测井曲线识别，研究其边界和内部样式等[16]。测井资料的局限性在于，它不能识别出MTDs的搬运方向及内部的具体形态，且深水钻井成本大，岩心资料少。因此本文主要利用高精度的三维地震资料，通过对MTDs的地震剖面、平面、三维模拟来具体识别其特征与展布。
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图 2 琼东南盆地陵水凹陷陆坡典型剖面Figure 2. Type sections through the slope of Lingshui Sag,Qiongdongnan Basin根据北康盆地第四纪沉积地层，MTDs在地震剖面上外部呈连续性差、弱振幅的丘状、波状反射特征，内部表现为杂乱、空白、弱-中-强振幅的反射特征；在尼日尔三角洲盆地和珠江口盆地的深水地层中可见MTDs呈半透明、低振幅、杂乱反射特征[7,16]。本文通过研究陵水凹陷陆坡区高分辨率三维地震资料，识别出研究区MTDs有以下特征：① 在地震剖面上MTDs呈平行或亚平行状的弱振幅、杂乱、丘状反射特征；② 研究区处于块体搬运沉积体系体部-趾部区域，因此在研究区识别出逆冲推覆构造，在剖面上通常表现为多个叠瓦状的逆冲断层和一系列挤压脊（图2）；③ 在平面上呈长条形—似扇状几何特征（图3），在构造图上可以看到凹陷的区域就是MTDs对基底的侵蚀作用区（图1）。MTDs的岩性主要和陆坡头部垮塌下来的物质有关，深海披覆泥占大多数，并且在MTDs趾部主要是碎屑流沉积，因此在剖面图上可以看到杂乱反射主要为半透明反射特征。MTDs在搬运的过程中本身对下伏地层会有侵蚀作用，因此下伏地层的地震反射会弱于顶界面地震反射[14-15]。MTDs会遭到海底地形的控制，还会受到水道和底流作用的改造，因此它的顶界面通常为不规则起伏形态（图2a）[3,13]。顶界面接着被后来的各种沉积物所填充[17]。块体搬运沉积（MTDs1）对下伏地层的侵蚀作用会形成残余地层，MTDs的侵蚀强度和下伏地层岩性决定了残余地层的规模和分布（图2）。研究区主要是MTDs体部和趾部区域，在地震剖面上常见逆冲构造，逆冲构造以连续的弧形向下坡方向搬运（图1，图2）。
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图 3 MTDs1均方根属性图（a）和瞬时频率图（b）Figure 3. RMS amplitude map of MTDs1(a)， instantaneous frequency map of MTDs1(b)在深水重力沉积体系中，水道堤岸复合体也是重要组成部分，水道是沉积物向深海区搬运的主要通道和沉积填充区域[18]。浊积水道主要在MTDs顶界面形成，它分为侵蚀期和填充期[19]。侵蚀期的水道主要对MTDs顶界面进行侵蚀，一般很少发生沉积作用；填充期时，水动力条件减弱，在水道内部发生沉积，在水道外侧形成堤岸沉积（图2）。因此在形成MTDs顶界面不规则起伏形态时，水道的侵蚀作用也是重要的因素。
2.1 侵蚀擦痕
侵蚀擦痕一般多发育于MTDs的体部和趾部，由头部所滑塌下来的块体在体部逐渐卸去重力，在体部其重力作用慢慢减弱，物源所携带的物质在此处逐渐沉积[4,8]。沉积物从头部滑动，顺着陆坡向下搬运到体部时逐渐转化为碎屑流[14]。这些碎屑流沉积物由自身重力作用继续沿着基底剪切面向下搬运，会侵蚀水道壁和下伏地层。块体搬运过程中的动力强弱决定了侵蚀擦痕发育的数量和大小，动力越强，块体对下伏地层的侵蚀性越强，侵蚀擦痕越大。由于MTDs在体部的侵蚀作用较强，基底剪切面会受到侵蚀，形成比较常见的剪切槽。研究区发育的侵蚀擦痕显示，它下伏地层的同相轴被断开，侵蚀擦痕内部为杂乱或空白反射，呈波状弱连续地震相特征（图4）。在平面上，侵蚀擦痕表现为不规则的凹槽，图中凹凸不平的表面证实了块体在搬运过程中对下伏地层具有侵蚀性（图1）。侵蚀擦痕较为平直，其宽度大约为1～2 km，MTDs的强度和下伏地层的岩性决定了侵蚀擦痕的规模（图3）。
2.2 逆冲推覆构造
逆冲推覆构造与大型的逆冲断层不同，它是发育在块体搬运沉积的趾部，并且在挤压作用下形成的叠瓦状排列。块体在向下坡方向搬运的过程中由于地形的影响而受到限制，或后面的块体加速挤压前方块体使地层变形，这两种情况是形成逆冲推覆构造的主要动力因素[20]。逆冲推覆构造的规模取决于MTDs沉积体的大小和挤压动力强弱，沉积体的规模越大、挤压作用越强，其内部逆冲推覆构造发育的规模也越大，MTDs趾部逆冲构造的厚度一般达到数十米，有的甚至几百米厚[7]。从研究区逆冲推覆构造典型剖面观察发现，MTDs内部逆冲推覆构造的同相轴表现为中—低振幅且连续的波状反射特征，它一般都是叠瓦状排列并且弯曲方向与块体搬运方向一致（图5）。在平面上，逆冲构造的特征为厚度较大的长条形脊，块体滑塌的方向垂直于逆冲脊（图1）；均方根振幅图和瞬时频率图上显示，逆冲构造发育区为连续的条带状，并向块体搬运方向凸出（图3）。从图5可以看到，由于MTDs后期受到的挤压作用较强，因此MTDs顶界面的振幅一般要强于底界面。
2.3 挤压脊
挤压脊的发育位置比较广泛，在深水环境和陆地都有发育[7]。挤压脊的发育规模受到陆坡坡度和MTDs底部地形的控制，坡度较大或者地形隆起会使块体向前搬运时受阻，地层会受到更严重的挤压作用，容易形成规模较大的挤压脊。挤压脊一般都与逆冲推覆构造一起出现，挤压脊是由于MTDs受到挤压作用时，外部形态会变得起伏不平，后期地层继续发育时就会受到MTDs的影响。挤压脊多发育于挤压作用强烈的趾部区域。研究区的地震剖面显示，挤压脊隆起的区域正是逆冲构造向上抬升的位置，在MTDs的顶界面还可以看到脊和谷会交替出现，谷的位置就是后期浊流最先填充的区域（图6）。在平面上，挤压脊的现象与逆冲推覆构造相似，构造图中表现为地形局部隆起形成连续凹凸不平的表面（图1）；瞬时频率图中显示为连续的弧形并且沿着块体搬运方向倾斜（图3b）。
3. MTDs与后沉积地层关系
陆坡由于失稳、垮塌等原因形成的MTDs在搬运过程中会侵蚀下伏地层并且边搬运边沉积，MTDs沉积后所形成的海底地形，还可以影响后期浊流的走向和浊流沉积的分布[21]。这些直接或间接地影响了后期地层的发育和沉积物的流动方向。MTDs1和MTDs2的地层直接接触，即MTDs1的顶界面为MTDs2的底界面（图7）。MTDs1的地层沉积薄厚不一，在下伏地层隆起的区域MTDs1的沉积少，地层相对较薄（图7）。通过剖面可以看到，MTDs1沉积厚度较薄的区域，其上部的浊流沉积地层则相对较厚（图8）。在层间也有部分区域发育连续性较好的地震反射，这块连续性较好的地层有可能是浊流沉积的产物，表明了块体搬运沉积在继续向坡下运动时会逐渐向浊流沉积转化，重力流作用下的块体搬运沉积不是时刻发生，在构造作用减弱的区域会发育较为连续的地层[22]。MTDs1的现今地貌图显示有许多凸起和凹陷的区域，并且还有一些弓形的脊，这些长约10～15 km、宽约2～3 km的逆冲脊主要发育在逆冲构造形成的区域（图9a）。MTDs1主要通过起伏不平的顶界面对后期浊流沉积产生控制作用和影响，这些凸起和凹陷会影响后期地层沉积的厚度和沉积物的流向，这些脊也会阻碍和抑制后期沉积物的下坡运动。
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图 7 MTDs与后期浊流沉积的典型剖面Figure 7. Typical sections showing MTDs and late turbidity deposition![]()
图 8 东北方向上后期浊流沉积的典型剖面Figure 8. Typical sections showing late turbidity current deposition in the northeast![]()
图 9 MTDs与后期浊流沉积属性图Figure 9. attribute map of MTDs and later turbidity current depositsa. Current geomorphology of MTDs1, b. thickness map of turbidity current deposits between MTDs1and MTDs2, c. thickness map of MTDs2, d. the root mean square attribute map of turbidity current deposits.MTDs1之上是一期浊流沉积地层，浊流沉积发育的地层相较于MTDs的地层连续性好，呈中—强反射特征（图7，图9d）。浊流沉积厚度图的西南低洼区域显示，浊流在此区域内沉积较少，可能的原因是下伏MTDs1向上隆起或上覆MTDs2在搬运时侵蚀作用较大，侵蚀了原本已经沉积的地层（图7，图8a-b，图9b）。MTDs1顶界面逆冲脊的区域内地形起伏较大，脊与脊之间也可作为后期浊流的“通道”，这些通道作为浊流沉积物搬运的载体又叫浊积水道，浊积水道内部的振幅强于普通的浊流地层（图7-9）。这些逆冲脊不仅可以作为浊流的通道，而且也会抑制浊流的下坡运动，改变浊流流向，浊流顺着这些脊向地形低处继续运动沉积[22]。在MTDs1东南角区域内，其沉积较薄，地层凹陷，地形相较于前期较低，因此后期的浊流在此处沉积的地层较厚，其后的MTDs2却沉积较薄（图8e-f，图9）。在此处浊流沉积的地层中还发现了混合流，它是同一重力流事件中流体转化为多种不同性质流体的产物，即碎屑流沉积与浊流沉积，混合流的地层连续性比块体搬运沉积好，但比浊流沉积差（图7）。浊流沉积的地层除了受到下伏MTDs1顶界面起伏地形的控制和影响，还受到上覆MTDs2侵蚀作用的影响。当MTDs2的侵蚀作用变强，会对已经沉积的浊流沉积造成侵蚀，改变浊流沉积的地层厚度（图8a-b、e-f）。当浊流沉积的地层厚度改变后又会反过来影响MTDs2的后续沉积，因此这些控制作用都是相互影响的。
从整体来看，因为MTDs1沉积的厚度分布不一，就形成了起伏不平的顶界面，海底凹凸不平的地形以及那些狭长的槽状地形会影响甚至改变后续浊流的走向及其沉积分布。MTDs1的滑塌方向与后期浊流的流向并不一致，MTDs1的滑塌方向是垂直于它所形成的逆冲脊，而后期浊流的方向会随着地形不断改变（图9a，图10a-b）。后期浊流沉积显示，在MTDs1沉积厚、地形较高的区域浊流沉积较薄，在MTDs1沉积较薄的区域浊流沉积的地层厚（图9a-b，图10）。浊流沉积的地层起伏也会受到MTDs1的地形控制，在浊流刚沉积时，会首先填充MTDs1表面低洼区域，之后填充沉积相对较平的地层。MTDs1一些局部的突起太高，后期的浊流沉积并不能完全覆盖这些隆起（图7，图10c），就会造成MTDs1直接与后期MTDs2接触并对其产生影响和控制作用（图10b-c）。到MTDs2沉积时，浊流沉积的地层对其起主要的控制作用，它沿着浊流沉积的表面逐渐沉积，先是在低洼处大量沉积然后再向周围扩散沉积，并且MTDs遇到下伏地层凸起处会受到地层影响而改变其自身形态。MTDs的侵蚀能力会使MTDs2侵蚀下伏的浊积地层，使下伏地层缺失并厚度减薄，而自身的厚度增加。因此在浊流沉积较厚的区域，MTDs2沉积较薄；在浊流沉积较薄的区域，MTDs2沉积较厚；MTDs2的厚度会随着浊流沉积的起伏而分布不一（图9b-c，图10）。
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图 10 MTDs1对后期浊流和MTDs2的控制作用Figure 10. The control of MTDs1 on the late turbidity current and MTDs2MTDs顶面凸起的区域限制了浊流的继续流动，改变浊流流向，使其顺着凸起边缘向地势较低处继续搬运沉积。在其顶面低洼的区域，如两脊之间的洼陷则充当了浊流的通道，使浊流由通道向地形低处继续搬运沉积。浊流会不断因为MTDs地形的起伏而改变其流向，地形高处抑制其搬运，优先填充地形低处。当后期浊流沉积途径MTDs的起伏地形时，会受到变形速率、泥沙供给、水流动力等的影响，因此浊流的流向与其沉积分布会广泛受到MTDs起伏不平的地层控制。
4. 结论
（1）研究区所发育的深水重力流沉积单元包括块体搬运沉积体系、浊流沉积、水道堤岸复合体。
（2）研究区MTDs总体表现为弱振幅、低连续、杂乱或空白的地震反射特征且具有明显的侵蚀作用。在研究区识别出MTDs体部区域发育大量侵蚀擦痕，其地震相特征为波状弱连续；以挤压作用为主的MTDs趾部区域多发育逆冲推覆构造和挤压脊，呈中—弱振幅、中—低连续的丘状地震反射特征。
（3）研究区识别出两期MTDs分别为MTDs1和MTDs2。MTDs1在趾部挤压区域发育的逆冲脊长约10～15 km、宽约2～3 km，逆冲脊的发育改变了海底地形。通过对MTDs内部结构和MTDs起伏不平的顶界面的分析发现，MTDs内部结构的变化造成其顶界面的凸起与凹陷，顶界面的起伏变化控制了后期浊流流向，且进一步影响了浊积岩的厚度和分布。
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