内蒙古半干旱草原土壤水分对降水格局变化的响应

doi:10.17521/cjpe.2015.0155

摘要/Abstract

摘要：

在全球气候变化背景下, 未来我国北方半干旱地区的降水格局将呈现出季节与年际间降水波动增强和极端降水事件增加的趋势。水分是半干旱草原的主要限制因子, 降水格局变化导致的土壤水分状况的改变必然对生态系统的结构和功能产生显著的影响。该研究选取内蒙古多伦和锡林浩特两个典型半干旱草原群落, 通过分析2006-2013年的降水和多层次土壤(0-10 cm, 10 cm, 20 cm, 30 cm和50 cm)含水量连续观测数据, 研究降水格局变化对土壤水分状况及其垂直分布的影响, 特别是土壤水分对降水事件的脉冲响应过程。结果表明: 两个站点的土壤含水量均呈现显著的季节及年际间波动, 其中土壤表层 0-10 cm水分波动更剧烈。锡林浩特50 cm处土壤含水量波动较大, 主要由于春季融雪的影响。年际间多伦和锡林浩特生长季土壤表层0-10 cm土壤含水量与降水量存在显著的正相关关系, 下层(10-50 cm)土壤含水量与降水量相关性不显著。研究发现小至2 mm的降水事件就能够引起两个站点表层0-10 cm土壤含水量的升高, 即该地区有效降水为日降水量> 2 mm。表层0-10 cm土壤含水量对独立降水事件的脉冲响应可通过指数方程很好地拟合。降水事件的大小决定了降水后表层0-10 cm土壤含水量的最大增量和持续时间, 同时这个脉冲响应过程还受到降水前土壤含水量的影响, 但该过程中并未发现植被因子(叶面积指数)的显著影响。降水后水分下渗深度及该深度的土壤含水量增量主要由降水事件的大小主导, 同时受到降水前土壤含水量的影响。在多伦和锡林浩特, 平均每增加1 mm降水, 下渗深度分别增加1.06和0.79 cm。由此作者认为, 在内蒙古半干旱草原, 降水事件大小和降水前土壤干湿状况是影响土壤水分对降水响应的主要因素, 而植被因子的影响较小。

关键词: 降水事件, 降水格局, 脉冲响应, 半干旱草原, 土壤水分

Abstract:

Aims Under global climate change, precipitation patterns were predicted to change with larger seasonal and annual variations and more extreme events in the semiarid regions of northern China. Water availability is one of the key limited factors in semiarid grasslands. Changes in precipitation patterns will inevitably affect ecosystem structure and function through soil water condition. Our objective was to investigate the response of soil water content to changes of precipitation pattern, especially its pulse response to precipitation events.
Methods Two semiarid steppe sites (Duolun and Xilinhot) in Nei Mongol were chosen and meteorological stations were installed to monitor precipitation and soil volumetric water content (VWC) at five soil depths (0-10 cm, 10 cm, 20 cm, 30 cm, 50 cm) from 2006 to 2013. The pulse response of VWC at 0-10 cm to an individual precipitation event was simulated by an exponential equation.
Important findings Significant seasonal and inter-annual variations of VWC were observed at the Duolun and Xilinhot sites. VWC at 50 cm soil layer in Xilinhot showed an obvious increase during the early spring due to the influences of snow melting. Mean surface (0-10 cm soil layer) VWC was significantly correlated with annual precipitation across eight years, but VWC in the deeper soil layers (10-50 cm) were not impacted by precipitation. We also found that the precipitation event larger than 2 mm could induce a significant increase in surface (0-10 cm soil layer) VWC, and could be regarded as an effective precipitation in this region. The maximum increment of surface VWC after the events and lasting time (T_lasting) were determined by the event size, while showed negatively linear correlations with the initial soil water content before the events. Vegetation development (leaf area index) did not show significant impacts on the responses of surface soil moisture to precipitation pulses. The infiltration depth of rain water was also determined by rain size and pre-event soil moisture. In average, soil water can infiltrate 1.06 cm and 0.79 cm deeper in Duolun and Xilinhot with 1 mm more precipitation, respectively. Therefore, our results suggest that the event size and pre-event soil moisture were the most important factors affecting response patterns of soil moisture to rain events in semiarid ecosystems.

Key words: precipitation events, precipitation patterns, pulse responses, semiarid grassland, soil moisture

陈敏玲, 张兵伟, 任婷婷, 王姗姗, 陈世苹. 内蒙古半干旱草原土壤水分对降水格局变化的响应. 植物生态学报, 2016, 40(7): 658-668. DOI: 10.17521/cjpe.2015.0155

Min-Ling CHEN, Bing-Wei ZHANG, Ting-Ting REN, Shan-Shan WANG, Shi-Ping CHEN. Responses of soil moisture to precipitation pattern change in semiarid grasslands in Nei Mongol, China. Chinese Journal of Plant Ecology, 2016, 40(7): 658-668. DOI: 10.17521/cjpe.2015.0155

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链接本文: https://www.plant-ecology.com/CN/10.17521/cjpe.2015.0155

https://www.plant-ecology.com/CN/Y2016/V40/I7/658

图/表 11

表1 多伦和锡林浩特两个研究站点的基本信息

Table 1 General information of Duolun and Xilinhot sites

站点 Site	经纬度 Longitude and latitude	海拔 Altitude (m)	平均年降水量 Mean annual precipitation (mm)	年平均气温 Mean annual temperature (℃)	土壤类型 Soil type	群落高度 Plant community height (cm)	地上生物量 Aboveground biomass (g·m^-2)	优势植物 Dominant species	土地利用类型 Land use type
多伦 Duolun	42.05° N, 116.28° E	1 350	380	2.2	栗钙土 Chestnut soils	42	174	冷蒿 Artemisia frigida 克氏针茅 Stipa krylovii	2001年围封 Fenced from 2001
锡林浩特Xilinhot	43.55° N, 116.67 E	1 250	332	0.84	栗钙土 Chestnut soils	48	185	羊草 Leymus chinensis 大针茅 Stipa grandis	2005年围封并打草 Fenced and clipped from 2005

图1 表层0-10 cm土壤含水量(VWC0-10, y)对降水事件的脉冲响应模式图(参考Liu et al., 2002)。a和b, 方程的参数; PPT, 降水事件, 箭头指示降水事件发生的时间; Tlasting, 脉冲响应的持续时间(降水后VWC0-10高于VWCPre的时间); ΔVWC0-10, 降水后VWC0-10的最大增量; VWCMax, 降水后VWC0-10能够达到的最大值; VWCPre (y0), 降水前一天的VWC0-10。

Fig. 1 Conceptual model of the pulse response of surface soil water content (VWC0-10, y) to precipitation events (refer to Liu et al., 2002). a and b, parameters of the equation; PPT, precipitation event, the arrow indicates the time when PPT occurred; Tlasting, the lasting time of pulse response (the periods of VWC0-10 above VWCPre after the PPT); ΔVWC0-10, maximum increment of VWC0-10 after the PPT; VWCMax, maximum VWC0-10 after the PPT; VWCPre (y0), VWC0-10 of the day before the PPT.

图2 多伦(DL)和锡林浩特(XL)两个站点8年(2006-2013年)环境因子和植被因子月均值的动态变化(平均值±标准误差, n = 8)。A, 多伦平均月降水(柱形图)和气温(折线图)的季节变化。B, 锡林浩特平均月降水(柱形图)和气温(折线图)的季节变化。C, 多伦(DL)和锡林浩特(XL)月平均叶面积指数(LAI)的季节变化。

Fig. 2 Monthly means of environmental and vegetation factors across eight years (2006-2013) at Duolun (DL) and Xilinhot (XL) sites (mean ± SE, n = 8). A, Seasonal variations of mean monthly precipitation (bar) and air temperature (line) of Duolun. B, Seasonal variations of mean monthly precipitation (bar) and air temperature (line) of Xilinhot. C, Seasonal variations of mean monthly leaf area index (LAI) at Duolun (DL) and Xilinhot (XL).

图3 多伦(A)和锡林浩特(B)两个站点生长季不同土层平均土壤含水量(点线图)和降水量(柱形图)的年际变化(2006- 2013年)。

Fig. 3 Inter-annual variations of precipitation (bar) and soil water content (VWC) during the growing season at different soil depths (scatters and lines) at the two sites (A, Duolun; B, Xilinhot) from 2006 to 2013.

图4 多伦(A)和锡林浩特(B)两个站点降水量与生长季平均表层土壤含水量(VWC0-10)的关系。GSP, 生长季降水量; AP, 年降水量。*, p < 0.05。

Fig. 4 Relationships between surface soil water content (VWC0-10) and precipitation during the growing season at the two sites (A, Duolun; B, Xilinhot). GSP, the growing season precipitation; AP, annual precipitation. *, p < 0.05.

图5 多伦(A)和锡林浩特(B)两个站点不同土层日均土壤含水量(VWC)与反照率的动态变化(2006-2013年)。

Fig. 5 Seasonal dynamics of mean daily mean soil water content (VWC) at different soil depths and albedo at the two sites (A, Duolun; B, Xilinhot) from 2006 to 2013.

表2 降水后表层土壤含水量最大增量(ΔVWC0-10)和持续时间(Tlasting)的多元逐步回归分析结果

Table 2 Results of the multiple stepwise regressions on increment of surface soil water content (ΔVWC0-10) and lasting time (Tlasting) after the precipitation event at the two sites

因变量 Variable	站点 Site	进入变量 Entered variable	移除变量 Removed variable	参数估计 Parameter estimate	偏R² Partial R²	模型R² Model R²	p
ΔVWC_0-10	多伦 Duolun	方程截距 Intercept		2.32
		PPT		0.38	0.73	0.73	<0.001
		VWC_Pre		-0.19	0.06	0.79	<0.001
			ST_Pre	-0.08	0.00	0.79	0.282
			LAI	1.30	0.00	0.79	0.340
	锡林浩特 Xilinhot	方程截距 Intercept		0.92
		PPT		0.35	0.52	0.85	<0.001
		VWC_Pre		-0.08	0.08	0.01	0.084
			ST_Pre	0.01	0.00	0.86	0.820
			LAI	0.58	0.00	0.86	0.356
T_lasting	多伦 Duolun	方程截距 Intercept		11.63
		PPT		0.33	0.33	0.33	<0.001
		VWC_Pre		-0.42	0.22	0.55	<0.001
		ST_Pre		-0.17	0.05	0.60	0.011
			LAI	0.74	0.00	0.60	0.680
	锡林浩特 Xilinhot	方程截距 Intercept		6.53
		PPT		0.31	0.52	0.52	<0.001
		VWC_Pre		-0.27	0.08	0.60	0.003
			ST_Pre	-0.00	0.00	0.60	0.997
			LAI	0.95	0.00	0.60	0.502

图6 多伦(DL)和锡林浩特(XL)两站点降水脉冲响应过程的表层0-10 cm土壤含水量最大增量(ΔVWC0-10), 持续时间(Tlasting)和降水事件大小(PPT), 降水前土壤含水量(VWCPre)之间的关系。A, ΔVWC0-10和PPT的关系。B, Tlasting和PPT的关系。C, ΔVWC0-10和VWCPre的关系。D, Tlasting和VWCPre的关系。E, 单位降水引起的表层土壤水分增量(ΔVWC0-10 /PPT)和VWCPre的关系。***, p < 0.001; *, p < 0.050; #, p < 0.100。

Fig. 6 Relationships of the maximum increment of surface 0-10 cm soil water content (ΔVWC0-10) and lasting time (Tlasting) in the pulse response process to precipitation with precipitation event size (PPT) and soil moisture content before precipitation events (VWCPre) at the two sites (DL, Duolun; XL, Xilinhot). A, Relationship between ΔVWC0-10 and PPT. B, Relationship between Tlasting and PPT. C, Relationship between ΔVWC0-10 and VWCPre. D, Relationship between Tlasting and VWCPre. E, Relationship between the maximum increment of ΔVWC0-10 induced by 1 mm precipitation and VWCPre. ***, p < 0.001; *, p < 0.050; #, p < 0.100.

图7 多伦(DL)和锡林浩特(XL)两站点降水后土壤水分下渗深度(Depth)与降水事件大小(PPT)及降水前土壤含水量(VWCPre)的关系。A, Depth与PPT的关系。B, 单位降水入渗深度(Depth/PPT)与VWCPre的关系。***, p < 0.001; **, p < 0.010。

Fig. 7 Relationships between infiltration depth (Depth) with precipitation event size (PPT) and soil water content before the events (VWCPre) at the two sites (DL, Duolun; XL, Xilinhot). A, Relationship between Depth and PPT. B, Relationship between infiltration depth of 1 mm precipitation (Depth/PPT) and VWCPre. ***, p < 0.001; **, p < 0.010.

表3 不同土层降水后土壤水分增量(y, %)与降水事件大小(x, mm)的线性回归分析结果(包括回归方程, R2和p值)

Table 3 Results of linear regression (including equation, R2 and p value) between precipitation event size (x, mm) and the increment of soil water content (y, %) at different soil depth

土层 Soil layer (cm)	多伦 Duolun				锡林浩特 Xilinhot
土层 Soil layer (cm)	方程 Equation	样本量 No. of samples	R²	p	方程 Equation	样本量 No. of samples	R²	p
10	y = 0.31x - 0.37	40	0.54	<0.000 1	y = 0.39x - 0.91	40	0.72	<0.000 1
20	y = 0.20x + 0.44	14	0.34	0.029 8	y = 0.34x - 3.45	17	0.67	<0.000 1
30	y = 0.38x - 7.56	7	0.77	0.009 4	y = 0.27x - 4.12	5	0.77	0.051 3

图8 多伦(DL)和锡林浩特(XL)两站点土壤容重垂直分布(0-100 cm)。 *表示两个站点之间存在显著差异(p < 0.050, n = 5)。

Fig. 8 Vertical distributions of soil bulk density (0-100 cm) at the two sites (DL, Duolun; XL, Xilinhot). * indicates significant difference between the two sites at p < 0.050 (n = 5).

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