2016, Vol.36
② 南京大学地理与海洋科学学院, 南京 210046;
③ 江苏省气候变化协同创新中心, 南京 210093)
利用高分辨率气候代用指标重建古环境演变是当今全球变化的重要研究内容[1]。中国第四纪环境变化研究中磁化率、有机碳、碳酸盐、同位素、孢粉、藻类、植硅体等作为气候代用指标已被广泛研究并取得丰硕成果[2～13]。沉积物颜色是沉积环境综合作用的结果，近年来许多研究者在沉积环境的研究中将色度作为气候代用指标。色度指标体系基于门赛尔表色系统(CIE1976(L *、 a *、 b *))，该系统于1905年由Munsell提出[14]，使用亮度(L *)、红度(a *)和黄度(b *)3个指标描述颜色空间[14～16]。L *变化于黑(0)和白(100)之间，主要受有机质和碳酸盐的影响；a *变化于红和绿之间(＋a *代表红色方向，-a *代表绿色方向)，b *变化于黄和蓝之间(＋b *代表黄色方向，-b *代表蓝色方向)，a *和b *主要与针铁矿、赤铁矿等有关，a *和b *值越高表示氧化作用越强，反之氧化作用越弱[17～24]。因此，色度可以作为环境重建的代用指标。目前，色度在不同沉积物研究中均有应用。黄土中a *整体上呈现由北向南增高的趋势，与中国土壤发育程度随纬度降低不断增强的变化模式一致[25, 26]。朱丽东等[27]在对金衢盆地网纹红土研究中使用了色度指标，表明网纹红土因其特殊斑纹结构而具特殊的色度表达系统，红白网纹的色差能够表示网纹发育程度及其发育的阶段性；Helmke等[28]通过对北大西洋沉积物色度记录的研究，揭示了过去50万年千年尺度气候变化模式，并指出海洋沉积物a *的变化或许与气候变化引起浮冰碎屑中陆源含铁等致色矿物的变化有关；吴艳宏和李世杰[17]对湖泊沉积物色度进行了研究，发现湖泊沉积物中L *与沉积物碳酸盐含量正相关，a *与沉积物中Mg含量正相关，b *与三价铁含量正相关并能够反映湖水深度变化。本文试图通过对位于杭嘉湖平原北湖桥钻孔(BHQ)沉积物色度记录的研究，初步探讨该区域早-中全新世环境变化特征。
2 区域地理概况BHQ孔位于杭嘉湖地区(图 1a和1b)，对全新世气候变化敏感，曾多次出现海侵与海退现象[29]，并且古人类遗址分布广泛[30, 31]。杭嘉湖平原全新世地层一般分布在长三角第一硬土层之上，以灰色、深灰色浅海、滨海相以及潟湖和湖沼相沉积为主[32]。有研究表明该区海平面上升最大速率发生在约7.0cal.ka B.P.以前[33]，在这之前该区水域范围较大、水位较高，之后水位大幅下降，海岸线迅速后退，除一些低洼处为沼泽或河湖相沉积外，高地均出露地表，同时人类文明也在该区域开始发展，5.0cal.ka B.P.左右的良渚文化时期杭嘉湖平原已全部成陆并接近现今面貌[29, 34～36]。该地区地势低平，平均海拔为2～4m[37]，水系较发达，河网密布，主要河流是发源于天目山的东苕溪。气候属东亚季风气候，雨热同期。多年均温为15～16℃，年均降水量为1000～1400mm[38]。
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图 1 杭嘉湖平原(a, b)及采样点位置(c)示意图 Fig. 1 Location of Hangjiahu Plain(a, b) and sampling site(c) |
BHQ孔(30°22.443′N，119°56.237′E)位于浙江省杭州市余杭区瓶窑镇(图 1c)，打钻时间为2010年9月，孔号为ZK4，型号为100型，孔径为10cm，柱样长19m。由于距地表 0～4.775m未能获取连续柱样，故选择距地表 4.775～19.000m进行研究。
色度和粒度样品以2.5cm间隔共535块，总有机碳(TOC)样品以10cm间隔共136块。色度、粒度实验均在浙江师范大学地理与过程实验室完成。其中，色度采用CIE L *、 a *、 b *表色系统[14]，仪器为日本美能达公司生产的CR-400色彩色差仪。实验过程为： 1)取适量样品置于45℃的恒温干燥箱中烘干后碾磨均匀(保持样品颗粒在固结成团前原始大小)；2)进行仪器黑白校正；3)取2～3g碾磨的样品置于标准正白色板上，压实压平后在恒定背景光源环境下随机取3点进行测试并记录L *、 a *、 b *的3点滑动平均值。粒度使用英国Malvern仪器有限公司生产的Mastersizer2000型激光粒度仪测定，实验由李黎霞完成。TOC前处理由程龙娟完成，测定由国家海洋局第三海洋研究所稳定同位素质谱实验室完成，分析仪器为稳定同位素质谱仪(Delta V Advantage)，分析误差 < 0.2 ‰。
4 结果与分析 4.1 BHQ孔全新世沉积环境与年代序列BHQ孔岩性以灰色、灰黑色粉砂和粘土质粉砂为主，有些层夹植物碎屑、铁锰结核和钙结核等。根据样品粒度组成[39]，结合TOC百分含量变化，BHQ孔岩性与沉积环境分如下几段(图 2)：第一段(19～17m)为灰色、灰黑色粉砂质砂和灰色粘土质粉砂，粘土所占比例由下而上逐渐升高，砂百分含量降低，指示水量不断上升；该段TOC均值为0.49 ％，，但粘土质粉砂层TOC含量明显高于粉砂质砂层。综合粒度和TOC指标推断为湖沼相沉积环境。第二段(17.0～8.9m)为灰色、灰黄色粉砂，可分为上、下两个亚段：下亚段(17.0～12.7m)，相较第一段该段粘土含量急剧下降，砂含量上升，平均达到7.95 ％，反映出沉积环境发生剧烈变化。Wang等[40]的研究表明，长江以南、钱塘江以北8.6～8.5cal.ka B.P.期间发生了一次海平面快速上升事件，故推测本阶段研究区经历了由于海平面上升而引发的加积作用。上亚段(12.7～8.9m)为灰色粉砂，砂均值降低为0.97 ％，TOC平均值由下亚段的0.28 ％增加到0.46 ％，说明加积作用减弱，湖水位有一定上升。第三段(8.9～6.7m)为灰色粘土质粉砂，含植物碎屑，可见微弱的水平层理，粘土含量急剧上升；TOC均值达全孔最高(平均为0.95 ％)，推测湖水较深。第四段(6.700～4.775m)为灰色粉砂到灰色、灰黄色粘土质粉砂，可分为两个亚段： 6.70～6.15m粘土与TOC(平均含量为0.24 ％)含量均下降，推测湖水位下降，湖泊向沼泽演化；6.150～4.775m夹杂氧化度较高的黄色沉积，TOC平均含量仅为0.36 ％。相关研究表明[41]，良渚、瓶窑一带在良渚文化末期广泛存在厚度不一的泛滥沉积物——黄粉土沉积层，该沉积层岩性为粘土质粉砂，以黄色、黄褐色为主，与本钻孔6.150～4.775m沉积特征较相近，推测本段有可能由湖沼沉积环境逐渐转向泛滥沉积环境。
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图 2 BHQ孔与BHQ2孔年代、岩性、 TOC和粒度对比图 Fig. 2 The date, lithology, TOC and granularity contrast between cores BHQ and BHQ2 |
BHQ孔分批测定了7个14 C年代(表 1)，其中4块样品由美国迈阿密Beta分析实验室(Beta Analytic Inc)完成，其余均在北京大学核物理与核技术国家重点实验室加速器质谱实验室-第四纪年代测定实验室完成。BHQ孔共获得4个有效测年数据(图 2)。为弥补BHQ孔上部缺失之不足，2012年在距离原孔位置约500m处打平行孔BHQ2(图 1和图 2)。BHQ2孔有6个有效测年数据(表 1)，均由美国Beta实验室完成。所有14 C年代均使用OxCal程序校正到日历年龄。根据BHQ孔4个有效测年数据计算该钻孔各沉积层的沉积速率，反推其他各深度年龄[42, 43]，建立了BHQ孔年代序列，并与BHQ2孔进行了对比。推算结果显示，BHQ孔19.000～4.775m段年龄约为11.4～4.2cal.ka B.P.，对应于早-中全新世。
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表 1 浙江瓶窑镇BHQ与BHQ2钻孔14 C年龄和日历年龄 Table 1 Dating results of cores BHQ and BHQ2 in Pingyao area, Zhejiang Province |
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表 2 浙江瓶窑镇BHQ钻孔各段沉积物色度与粒度、 TOC相关性 Table 2 Sediment color correlation with granularity and TOC in different stages for core BHQ in Pingyao area, Zhejiang Province |
BHQ孔样品色度测量显示，L *值为53.09～72.79，平均值63.30；a *值为-0.84～6.45，平均值1.50；b *值为6.61～25.84，平均值10.79。各值的相关性分析结果显示(表 2)，a *与b *变幅及变化规律大体一致(图 3)。按照色度变化可以将BHQ孔沉积记录由下而上分为4段：
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图 3 BHQ孔色度、 CaO及TFe2O3随深度变化曲线 Fig. 3 Color, CaO and TFe2O3 content of core BHQ |
第Ⅰ段19～17m(11.4～8.7cal.ka B.P.)，L *为71.10～53.09(全孔最小值)，变幅达各阶段最大，平均为63.84；a *为3.36～1.33，其均值达到全孔最大(1.77)；b *为16.07～9.13，平均为11.43。
第Ⅱ段17.0～8.9m(8.7～8.0cal.ka B.P.)，L *为64.74～60.27，平均62.37；a *为2.98～1.11，平均1.44；b *为11.30～8.45，均值10.52。各参数均值与全孔均值相当，变化较稳定。
第Ⅲ段8.9～6.7m(8.0～5.7cal.ka B.P.)，L *为64.72～59.12，平均61.91；a *为2.42～0.07，平均1.41；b *为11.20～7.33，平均9.00。各参数变幅均较上段增大，且均值为全孔最小值。
第Ⅳ段6.700～4.775m(5.7～4.2cal.ka B.P.)，L *为72.79(全孔最大值)～59.6，平均67.76；a *为6.45～-0.84，平均1.54；b *为25.84～6.61，平均12.99。本段L *、 b *均值以及a *、 b *变化幅度均达全孔最大。
5 讨论 5.1 色度的古环境意义沉积物颜色受成岩时期沉积环境的影响，其影响因素主要包括有机质、碳酸盐和特定的化学成分等[18]。不同类型沉积物颜色的古环境意义存在差别，其成因较复杂[44～47]。现代黄土、红土和古土壤，L *与有机质含量呈负相关性[48～52]；湖泊与海洋沉积物，L *与碳酸盐含量呈正相关性，沉积物碳酸盐含量变化能有效地反映气候冷暖干湿变化：在暖气候背景下，有效湿度降低有利于碳酸盐沉积；在冷气候背景下，干旱的气候条件更有利于碳酸盐沉积[17, 22, 53～57]。苟仁错沉积物研究则表明，a *值反映了MgO含量变化，b *值与TFe2O3 ％呈较好正相关性，较高b *值代表较低湖面，反之亦然[17]。
用SPSS Statistics 17.0软件将BHQ孔色度指标与粒度、 TOC按照色度分段进行相关性分析(表 2)，结果表明，b *和L *与其他环境指标有较显著相关性，但变化较复杂。
如表 2所示，各段b *与TOC呈显著负相关性。由于TOC在湖泊沉积物中反映湖泊的初级生产力[58, 59]，不仅与温度有关，且湖面太低强氧化作用不利于有机碳的保存[60, 61]。因此，BHQ孔色度记录中较低b *值对应于较高湖面，这与吴艳宏和李世杰[17]的研究结果一致；另一方面，BHQ孔b *值与TFe2O3 ％正相关(图 3)，也说明b *能够反映湖水位的变化。
一般而言，L *与总有机碳含量负相关[20]或与碳酸盐含量正相关[17]。然而，BHQ孔L *与TOC相关性很低(表 2)，而与CaO ％负相关(r=-0.56)(图 3)。L *与粒度相关性较为复杂(表 2)，第Ⅰ、 Ⅲ段L *与粘土组分呈负相关，Ⅱ、 Ⅳ段则呈较显著正相关。由于Ⅰ、 Ⅲ两段粘粒组分百分含量较高，且为较稳定湖泊或沼泽沉积环境，因此L *高值代表较低水面；Ⅱ、 Ⅳ两段粘粒组分含量偏低，且受泛滥冲积影响较大，说明在不稳定的沉积环境下L *高值可能与较高水面有关。但由于L *控制因素较多，在进行环境判断时需参考其他环境指标。
5.2 研究区早-中全新世环境演变根据色度记录，结合粒度、 TOC、孢粉浓度和E/D(常绿树种％/落叶树种％)[42]等代用指标，可以将研究钻孔的早-中全新世划分为4个气候环境演变阶段(图 4)。
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图 4 BHQ钻孔沉积物色度、粒度、 TOC、孢粉总浓度以及E/D变化曲线 Fig. 4 The color index, granularity, TOC, spore-pollen concentration and E/D content of core BHQ |
第Ⅰ段，11.4～8.7cal.ka B.P.(19～17m)：b *均值(11.43)较高，指示研究区水位较浅，可分早、晚两个时段。早期(11.4～11.2cal.ka B.P.)L *和b *均值较高，分别为66.01和12.02，TOC平均含量(0.33 ％)偏低，对应孢粉浓度偏低[42]，砂平均含量(39.10 ％)偏高，表明气温与水位总体偏低。但TOC、粘土、孢粉浓度以及乔木花粉含量变化呈上升趋势[42]，L *和b *值的变化呈下降趋势(图 4)，指示气温与湖面逐渐升高，研究区已进入全新世回暖期。这种环境变化趋势与方修琦和侯光良[62]以及顾明光[63]的研究有较好一致性。晚期(11.2～8.7cal.ka B.P.)L *和b *均值分别下降为63.16和11.24，而TOC平均含量增加为0.53 ％，粘土平均含量达30.74 ％，砂平均含量急剧下降为0.80 ％，表明气候较早期进一步向暖湿发展，水位上升。上述色度记录与孢粉组合反映的环境变化较吻合，该时段早期地层中花粉浓度较低，而晚期花粉浓度急剧增加，其中乔木花粉含量由82.62 ％上升为85.43 ％，E/D呈波动上升趋势，在较干环境下生长的蒿属花粉含量也由早期的1.15 ％下降为0.71 ％ [42]，表明气候变暖湿。根据上述环境指标变化推测，研究区在8.7cal.ka B.P.前就步入全新世大暖期。虽然该推断与前人研究结果[64～71]有较好的相似性，但由于研究钻孔分辨率不够高，研究区步入全新世大暖期的准确时间有待进一步研究。
第Ⅱ段，8.7～8.0cal.ka B.P.(17.0～8.9m)：L *、 a *和b *均值分别为62.37、 1.44和10.52，与全孔均值接近，各环境指标波动较小。与第Ⅰ段相比，b *均值有所下降，推测水位略有增加；粘粒与TOC平均含量均急剧下降，分别为20.03 ％和0.37 ％。由于温度和降水量是影响植物生长的关键因素，故TOC含量常用来反映气温和湿度高低[60, 72]，从该段TOC平均含量的减少推测气候变得干冷，该推论得到孢粉资料的证实[42]。与第Ⅰ段晚期相比，该时段地层中孢粉浓度急剧降低，乔木花粉含量较第Ⅰ段下降了19.03 ％，其中落叶栎属和松属花粉浓度下降幅度较大，但8.4cal.ka B.P.左右开始，孢粉浓度和E/D出现较大幅度波动上升，其中上升最为明显的是乔木花粉浓度，尤其是适宜较温暖湿润环境的常绿栎＋栲属花粉，乔木花粉含量上升，草本花粉含量下降[42]。另一方面，沉积物组成中，砂平均含量由7.95 ％急剧下降为0.97 ％，粘土、 TOC的平均含量增加，表明8.4cal.ka B.P.开始气温与湿度逐渐升高。综上所述该时段可分早、晚两个时期：早期(8.7～8.4cal.ka B.P.)研究区可能发生了一个持续300年左右的干冷气候事件，是大暖期中的一个冷波动，对应时段董哥洞石笋δ 18 O变化也指示干冷气候[71]，叶玮等[73]对BHQ孔的碳氧同位素研究中也检测到这一冷波动；晚期(8.4～8.0cal.ka B.P.)气候再次逐步向暖偏湿发展，水位上升。
第Ⅲ段，8.0～5.7cal.ka B.P.(8.9～6.7m)：色度指标变幅不同程度上升，但L *、 a *和b *均值达全孔最低，分别为61.91、 1.41和9.00，表明研究区水位上升到最高。前人研究也显示[74]，邻近地区该时段存在大面积水域。从TOC来看，其平均含量急剧上升为1.01 ％，达到全孔最大，粘土平均含量高达34.33 ％，粉砂平均含量大幅度下降，砂平均含量下降为0.08 ％。适宜生长在温暖湿润条件下的常绿栎＋栲属花粉含量也达到全孔最高值，湿生草本莎草科和水生草本香蒲科百分含量明显升高，孢粉浓度和E/D值较前急剧大幅上升[42]。综合各项指标推断，该时段为研究区全新世大暖期鼎盛阶段。
第Ⅳ段，5.7～4.2cal.ka B.P.(6.700～4.775m)：b *均值达到全孔最大(12.99)，反映湖水变浅；与之对应，粘土和TOC含量有所下降，平均值分别为25.61 ％和0.32 ％，粉砂含量大幅度上升(73.26 ％)。但纵观全孔，反映温度变化的指标TOC、孢粉总浓度和E/D均值仍然偏高，说明当时温度有所下降，但并非很低，而b *均值的升高、粘土均值的下降则指示湿度明显降低。马春燕[38]和刘演[75]关于东苕溪平原和杭州湾顶部区域的相关研究也表明该时段水位变浅；花粉研究表明[42]，本段乔木含量下降，草本含量上升为全孔最高，适宜温暖湿润气候条件的常绿栎＋栲属花粉含量下降，莎草科和香蒲科含量也呈下降趋势，而较干气候下生长的蓼科呈上升趋势，指示湿度降低。水域面积的缩小和湿度的降低，为良渚文化发展提供良好条件。良渚文化的相关研究表明[34]，该时段良渚文化快速发展，后期由于水位上升、泛滥严重导致良渚文化衰落。另外，在气候波动的背景下，5.7～5.5cal.ka B.P.期间，出现本孔最高b *值(25.84)，TOC、孢粉浓度出现谷值[42]，粘土平均含量突然急剧降低为19.83 ％，砂出现峰值，推测为一个持续约200年的干冷事件，可能与全球[76]和其他地区[77, 78]的5.5ka B.P.冷气候事件有关。
6 结论(1) BHQ孔色度分析表明，黄度(b *)和亮度(L *)能有效指示环境变化。b *与TOC呈显著负相关性说明黄度高低能反映湖水位高低，较高b *则代表较低湖面；在稳定水环境中，L *高值代表低水位，但在本研究区L *变化较复杂，需结合其他环境指标共同讨论环境演变。
(2) 基于色度记录，结合粒度、 TOC和孢粉等指标综合分析表明，研究区11.4～4.2cal.ka B.P.时段古环境变化明显： 11.4～8.7cal.ka B.P.时段，b *均值偏高，但由早至晚呈逐渐降低的趋势，气候总体由偏干冷转向暖湿，湖水位逐步上升；8.7～8.0cal.ka B.P.时段，b *与L *均值较前有所降低，温度与湿度呈逐渐增加趋势，早期(8.7～8.4cal.ka B.P.)为持续了约300年的干冷气候事件，晚期(8.4～8.0cal.ka B.P.)气候再次逐步向暖偏湿发展，水位上升；8.0～5.7cal.ka B.P.时段，L *与b *均值达全孔最低值，TOC含量和E/D值达到最高，推测为全新世大暖期鼎盛期，期间湖水位达到最高；5.7～4.2cal.ka B.P.时段，b *均值达全孔最大值，气候有变干趋势，其中5.7～5.5cal.ka B.P.期间出现一次持续约200年的冷气候事件。
(3) 研究区可能于8.7cal.ka B.P.前便已经进入了全新世大暖期，延续至4.2cal.ka B.P.，但大暖期中气候并不稳定，期间存在明显的气候波动。大暖期前期气候暖湿，后期湿度有所下降。
(4) 研究区全新世环境变化对全球气候变化有较好的响应。8.7～8.4cal.ka B.P.和5.7～5.5cal.ka B.P.期间地层中存在冷事件的记录。
致谢: 感谢审稿专家和编辑部老师建设性的修改意见，使文章得以完善和最终发表!
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② College of Geographic and Oceanographic Sciences, Nanjing University, Nanjing 210046;
③ Climate Change and Collaborative Innovation Center Jiangsu Province, Nanjing 210093)
Abstract
An improved predicting of future climate variabilities and changes relies on high-quality data sets from the past, especially the Holocene.The Hangjiahu Plain, which is located in south of the Yangtze River and north of the Qiantang River, a part of the eastern coastal areas of China, is sensitive to the Holocene climate changes.During the Holocene, Hangjiahu Plain occurred transgressive and regressive for many times, and Neolithic sites distribute in this region widely.A drill core of lake-swamp sediment with depth of 4.775~19.000m was obtained from Beihuqiao (30°22.443'N, 119°56.237'E).The dating data by 14C method indicate that the core spans the period of 11.4~4.2cal.ka B.P.Based on 535 color and granularity samples at 2.5cm intervals and 136 total organic carbon(TOC) samples at 10cm intervals, climate and environment during the Early-Mid Holocene was reconstructed. According to the color evolution rule, it can be divided into four stages to discuss (11.4~8.7cal.ka B.P., 8.7~8.0cal.ka B.P., 8.0~5.7cal.ka B.P.and 5.7~4.2cal.ka B.P.).The color results were compared with granularity and TOC in each stage, which shows that the yellow degree index(b*) is markedly negative correlating with TOC, the correlation coefficient are -0.663, -0.719, -0.590 and -0.651, so that higher b* indicates lower effective humidity.In addition, in the stabilized water environment, brightness index (L*) is negative correlating with clay, so higher L* infers drier environment.Results of color, TOC, granularity, spore-pollen concentration and E/D(the percentage of evergreen/deciduous)analysis indicate that the study area has undergone significant environmental change.During 11.4~8.7cal.ka B.P., in the early of this stage(11.4~11.2cal.ka B.P.)the value of L* (66.01) and b* (12.02) are high but on a declining curve, the percentage of TOC(0.33%) is low but on the raise, showing that the climate was a bit of cold and dry but changing to become warmer and wetter; in the late of this stage(11.2~8.7cal.ka B.P.)the value of b* has declined 0.73%, the percentage of TOC has increased by 0.2% and the percentage of clay has increased to 30.74%, indicate that the climate gradually turned to warm and wet, and we think that the study area may enter the Holocene Megathermal before 8.7cal.ka B.P.During 8.7~8.0cal.ka B.P., according the lower percentage of TOC(0.37%) and clay(20.03%), the climate turned to steadily dry and cold which lasted about three hundred years in 8.7cal.ka B.P.to 8.4cal.ka B.P., and from 8.4cal.ka B.P.to 8.0cal.ka B.P., the percentages of sand is rapidly declined from 7.95% to 0.97%, the spore-pollen concentration and E/D value are increasing rapidly, indicating that the climate was warm and moisture.During 8.0~5.7cal.ka B.P., the lowest average of b*(9.00), the highest percentage of TOC(1.01%) and the fast growing percentage of clay(from 20.03% to 34.33%) show that the climate became warmer and wetter, indicating that this period is the warmest period in the Holocene Megathermal.During 5.7~4.2cal.ka B.P., the highest average of b*(12.99)and the rapidly declined of the percentage of clay(25.61%), show that the climate become dryer.During 5.7~5.5cal.ka B.P.the temperature began to decline and the study area appeared a cold event which lasted nearly two hundred years.