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据估计,到21世纪末,由于大气中的温室气体,特别是二氧化碳(CO2)浓度的增加,全球平均温度预计将增加2~7 ℃[1]。随着人们对气候变化和温室气体减排的越加重视,关于农田土壤固碳潜力的研究也日趋深入。而土壤作为一个巨大而且具有挥发性的潜在碳库,可以缓冲大气中二氧化碳浓度的增加。土壤碳库的微小变化,都可以引起大气二氧化碳浓度的显著变化[2]。例如,ESWARAN等[3]的研究显示,全球土壤有机碳储量0.1%的变化将导致大气中二氧化碳质量浓度10 mg·L-1的变化。而据推测,在2 m土层中的土壤有机质浓度增加5.0%~15.0%可使大气中的二氧化碳浓度减少16%~30%[4-5]。可见土壤碳库的稳定、增长或衰减都与大气二氧化碳浓度变化密切相关。此外,土壤有机碳库约占陆地总有机碳库的2/3,是大气碳库的2倍。土壤平均每年排放到大气中的二氧化碳约为化石燃料碳排放量的11倍,大气二氧化碳储量的10.0%[6]。由此可知:土壤碳库积累和变化直接影响全球的碳平衡,也是大气碳库和全球气候变化的主要原因[7],因此,土壤在稳定全球气候、减缓温室效应方面发挥着重要作用。在陆地生态系统中,碳汇功能体现在碳库的储量和积累率,而碳源则体现在碳的排放强度。土壤碳库的变化主要表现在土壤有机碳储量的变化上,土壤有机碳储量是进入土壤有机物质(生物残体等)的输入与损失(以土壤微生物分解作用为主)之间的平衡[8],而土壤有机碳的稳定性则主要体现在土壤有机碳周转期的长短。鉴于此,土壤中碳库的量化和稳定性机制引起了科学家的极大关注[9-10]。然而,在预测21世纪大气二氧化碳浓度时,土壤有机碳的稳定性是其不确定性的主要来源[11]。而提高土壤有机碳的稳定性可以使土壤以有机物的形式固定大气中更多的二氧化碳,有助于科学客观地预测土壤有机碳的动态变化等,提高土壤的碳汇功能。土壤有机碳的一个重要组成部分就是植硅体封存有机碳(phytolith-occluded organic carbon,PhytOC,以下简称植硅体碳),植硅体碳是植硅体在形成过程中封存在部分植物细胞中的有机碳。植硅体存在于多种植物细胞中,是高等植物通过吸收单硅酸,在细胞内或细胞间硅化沉淀形成的非晶质二氧化硅矿物颗粒。植硅体碳具有强稳定性,可在土壤中长期保存,稳定达数千年至万年之久,成为陆地土壤长期固碳的重要机制之一。植硅体封存有机碳是土壤中重要的有机碳种类,且作为生态系统碳汇的重要组成部分,关于其稳定性的研究,比如如何准确测定和评价植硅体碳的稳定性,以及采取优化管理措施来提高植硅体碳的稳定性等已引起各国科学家的注意。本文综述了土壤植硅体封存有机碳的形成机制与特征、植硅体碳稳定性研究的重要意义以及影响植硅体碳稳定性的因素。
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土壤有机碳的稳定性分为生物化学稳定性、化学稳定性和物理稳定性等。闭蓄在团聚体内和吸附矿物上的土壤有机碳(SOC)是物理保护机制[12]。
土壤团聚体分为大团聚体(>250 μm)和微团聚体(<250 μm)。2种团聚体的物理稳定性机制是不同的[12]。在有机质的实验分组方法中,物理分组方法最为普遍。物理分组方法包括颗粒大小分组(particle size fractionation)和相对密度分组(density fractionation)。前者根据有机碳与土壤中不同初级颗粒结合形成各级复合体将有机碳分成砂粒结合态有机碳(50~2 000 μm),粉粒结合态有机碳(2~50 μm)和黏粒结合态有机碳(<2 μm),而后者根据有机碳与土壤矿物结合的形态将有机碳简单分成轻组有机碳和重组有机碳[13-14]。
土壤颗粒态有机碳(particulate organic carbon,POC)是介于新鲜的动植物残体和腐殖化有机物之间的暂时或过渡的有机碳组分,是与砂粒结合的有机碳部分,在土壤中周转速度较快,比土壤总有机碳更易受土地利用方式的影响[15]。吸附矿物表面的有机碳,主要与不同粒级的矿物颗粒紧密结合,形成有机-无机复合体,使其矿化速率大为减慢,故这部分有机碳往往相对稳定[14]。
土壤中存在的安全碳的形态有物理性保护的有机无机复合体(如微团聚)、木炭和植硅体碳。植硅体碳的封存机制被认为是有机无机复合体抗化学溶解的物理保护作用[8],木炭的形成也可被认为是土壤碳的长期封存机制[16]。植硅体碳具有很高的抗氧化和抗分解能力,是最稳定而安全的碳的形态。可长期累积于土壤中达数千年至万年之久,因而成为陆地土壤长期固碳的重要机制之一[17-19]。
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土壤有机碳稳定性可用平均滞留时间(MRT)或周转期来量化。土壤有机碳中碳元素的周转一般是由输入和输出之间的平衡所决定。土壤有机碳的周转率通常用碳稳定状态的平均滞留时间(MRT)或半衰期(T1/2)来表示。碳的平均滞留时间可定义为稳定状态下碳平均滞留时间,也可定义为稳定状态下元素完全更新的时间。土壤有机碳的半衰期为现有碳库分解一半所需要的时间。
区分土壤中稳定态土壤碳和不稳定碳对于探明土壤碳稳定性的机制至关重要。由于土地利用或管理等变化引起了环境条件的改变,矿质土壤总有机碳含量须经过几十到几百年才能平衡。土壤中生物、化学和物理过程之间复杂的相互作用使得不同土壤有机碳成分具有不同的化学结构和分解速率,周转时间从几小时到近万年[11, 20]。依据周转速率的快慢把土壤有机碳分成易变碳库(labile carbon pool)和稳定碳库(stable carbon pool),或活性库(active pool),慢性库(slow pool)和惰性库(passive pool)。CENTURY SOM模型[20]则把土壤碳划分为活性库(active pool),慢库(slow pool)和被动库(passive pool),其平均滞留时间值分别为1.5,25.0和1 000 a。表 1列出了具有不同土壤有机碳周转期的碳库类型及其化合物。
表 1 根据MRT和相应的化合物分类所定义的土壤有机碳库[20-24]
Table 1. Pools of SOC defined according to MRTs and corresponding compound classes[20-24]
残留物类型 碳库类型 物质类型 平均滞留时间/a 碳氮比 化合物 凋落物 代谢 可分解的植物材料 0.1~0.5 10-25 单糖,氨基酸,淀粉 结构 — 24 100-200 多糖 土壤有机碳 活性碳库 微生物生物量 可分解的植物物质 1-2 —— 活的生物量,颗粒有机质,多糖 慢性碳库 抗性植物材料 15?100 10-25 木质化组织,蜡,多酚 被动碳库 腐殖化有机质 惰性有机质 500-5 000 7-10 腐殖物质,黏土,有机配合物,生物炭 植硅体碳 硅化有机碳 <200-13 300* — 糖类,蛋白质,类脂物 说明 *植硅体碳在土壤中的存留时间。
Research progress and forecast of phytolith-occluded organic carbon stability in soil
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摘要: 植硅体碳(phytolith-occluded organic carbon, PhytOC)是一个重要的长期(数千年)陆地碳组分,从而成为陆地土壤长期固碳的重要机制之一。植硅体碳的稳定性对全球陆地土壤碳库贡献比植硅体碳储量要大得多。综述了土壤植硅体碳的形成机制与特征,研究植硅体碳稳定性的重要意义以及影响植硅体碳稳定性的因素:不同植被类型产生的植硅体碳的稳定性存在显著差异,不同生长环境下同一植被类型的植硅体碳稳定性也存在差异;古土壤中的植硅体碳稳定性大于幼年中的土壤;植物植硅体的形态组合能够响应土壤盐碱浓度及pH值的变化;湿度和降水等影响植硅体的数量、大小、形态组合以及碳、氧同位素;大气二氧化碳浓度对植硅体的类型、大小比率等产生影响;植硅体的硅铝比值越低,稳定性越高。表1参90Abstract: As an important long-term terrestrial carbon fraction, the phytolith-occluded organic carbon (PhytOC) has become an important mechanism in the long-term terrestrial carbon sequestration. The contribution of PhytOC stability to the global terrestrial soil carbon pool is much greater than PhytOC stocks. The paper reviewed the formation mechanism and characteristics of PhytOC, the significance of studying the PhytOC stability, and the determinants of the PhytOC stability. PhytOC produced from different types of vegetations had significantly different stability. PhytOC produced from the same type of vegetations but under different growth environments also had different stability. The PhytOC in ancient soil was more stable than that in young soil. The morphological combinations of phytolith in plants were able to respond sensitively to saline-alkali concentrations and pH values in soil. The humidity and precipitation could affect the quantity, size, morphology, assemblages δ13C and δ18O of phytolith. The smaller the Si/Al ratio of phytolith was, the higher the stability would be.[Ch, 1 tab. 90 ref.]
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Key words:
- soil science /
- phytoliths /
- stability /
- PhytOC sequestration rate /
- determinant /
- review
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表 1 根据MRT和相应的化合物分类所定义的土壤有机碳库[20-24]
Table 1. Pools of SOC defined according to MRTs and corresponding compound classes[20-24]
残留物类型 碳库类型 物质类型 平均滞留时间/a 碳氮比 化合物 凋落物 代谢 可分解的植物材料 0.1~0.5 10-25 单糖,氨基酸,淀粉 结构 — 24 100-200 多糖 土壤有机碳 活性碳库 微生物生物量 可分解的植物物质 1-2 —— 活的生物量,颗粒有机质,多糖 慢性碳库 抗性植物材料 15?100 10-25 木质化组织,蜡,多酚 被动碳库 腐殖化有机质 惰性有机质 500-5 000 7-10 腐殖物质,黏土,有机配合物,生物炭 植硅体碳 硅化有机碳 <200-13 300* — 糖类,蛋白质,类脂物 说明 *植硅体碳在土壤中的存留时间。 -
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