Notice: Wiley Online Library will be unavailable on Saturday 30th July 2016 from 08:00-11:00 BST / 03:00-06:00 EST / 15:00-18:00 SGT for essential maintenance. Apologies for the inconvenience.
 Methane (CH4) emissions from the drawdown area of the Three Gorges Reservoir (TGR) have not been thoroughly investigated even though the drawdown area encompasses one third of the reservoir surface. In this study, CH4 emissions from different land uses were measured in the TGR drawdown area. The average diffusive CH4 emissions were 2.61, 0.19, 0.18, and 0.12 mg CH4 m−2 h−1 in rice paddies, fallow lands, deforested lands, and croplands, respectively, and were positively related to the duration of the inundated season among the latter three land uses. On average the drawdown areas studied here (except rice paddies) were sources in the inundated season (0.22 ± 0.26 mg CH4 m−2 h−1) and a sink in the drained season (−0.008 ± 0.035 mg CH4 m−2 h−1). The water level was the dominant factor that controlled whether the drawdown area was either inundated or drained, which in turn determined whether the drawdown area was a source or sink of CH4 emissions. The average diffusive CH4 emissions from the fallow lands, croplands, and deforested lands increased as the distance from the dam increased from Zigui (0.10 ± 0.15 mg CH4 m−2 h−1) to Wushan (0.15 ± 0.29 mg CH4 m−2 h−1) to Yunyang (0.24 ± 0.27 mg CH4 m−2 h−1), which could reflect different sediment characteristics and water velocities. The total CH4 emission from the drawdown area was estimated to range from 1033.5 to 1333.9 Mg CH4 yr−1, which would account for 42–54% of the total CH4 emissions from the water surface of TGR.
If you can't find a tool you're looking for, please click the link at the top of the page to "Go to old article view". Alternatively, view our Knowledge Base articles for additional help. Your feedback is important to us, so please let us know if you have comments or ideas for improvement.
 Methane (CH4) is the second most abundant greenhouse gas in the atmosphere, with a relative contribution of about 20% of the greenhouse effect, second only to carbon dioxide (CO2) [Wuebbles and Hayhoe, 2002]. At the molecular level, however, CH4 can absorb infrared radiation 22 times more efficiently than CO2 over 100 years, thus making it one of the most potent greenhouse gases [Zhuang et al., 2009]. The atmospheric CH4 concentration has more than doubled in the past two centuries [Frankenberg et al., 2005], which is mainly attributed to the effects of fossil fuel combustion, waste management, enteric fermentation, the incineration of biomass, and agricultural and natural wetlands [St. Louis et al., 2000; Marani and Alvalá, 2007]. While not officially acknowledged, artificial reservoirs have been recognized as an important anthropogenic source of CH4 [Duchemin et al., 1995; Soumis et al., 2004; Abril et al., 2005], with global estimates of 4 Tg yr−1 for CH4 or 6% of the total emissions from natural lakes [Barros et al., 2011].
 Several studies have measured CH4 emissions from the water surfaces of reservoirs located in boreal, temperate, and tropical regions [Huttunen et al., 2002; Abril et al., 2005; Demarty et al., 2009]; however, few reports are available on CH4 emissions from drawdown areas [Chen et al., 2009, 2011; Lu et al., 2011]. The drawdown area is the vegetated (or cleared) littoral zone at the edge of the reservoir that experiences cycles between inundation and drainage based on water level of the reservoir, due to seasonal cycles or hydroelectric operations. The drawdown areas in reservoirs are considered “hotspot” zones for CH4 emission [Juutinen et al., 2001; Chen et al., 2009]. Narrow littoral zones may even support most of the lake-wide CH4 release during open water season [Bergström et al., 2007], as was seen in other studies [Juutinen et al., 2003a, 2003b]. Thus drawdown areas are potentially important CH4 emission sources and contribute to any spatial variability observed in emissions.
 A previous study on the Three Gorges Reservoir (TGR) has already shown that newly created marshes in the drawdown area are important CH4 emitters [Chen et al., 2009]. However, only 11% of the TGR drawdown area is actually occupied by marsh/wetlands with the remaining area dominated by dry lands, such as the deforested lands, croplands, and fallow lands [Ye et al., 2006]. Compared with wetlands, dry lands are very minor CH4 sources [Jiang et al., 2009] and may even act as CH4 sinks [Iqbal et al., 2009]. Low CH4 emissions from flooded dry lands were reported recently on the scale of 0.29 ± 0.37 mg CH4 m−2 h−1 basing on six measurements in different seasons [Chen et al., 2011]. Lu et al.  argued that the drained dryland drawdown areas of TGR might emit lower CH4 emission compared with that reported by Chen et al. , due to the exposure of dry lands. The anaerobic conditions are crucial to CH4 production and transfer because CH4 is mineralized to CO2 by methanotrophic bacteria under aerobic conditions [Topp and Pattey, 1997]. As seasonal fluctuations in the water level cause an alternating cycle between inundated and exposed dry lands that would effect CH4 emissions, sufficient seasonal investigations of emissions from various drawdown land types are required to resolve the temporal and spatial variability. The above mentioned studies of TGR CH4 emissions were quite limited spatially and temporally, and the environmental factors leading to these emission variations were not robustly analyzed [Chen et al., 2009, 2011; Lu et al., 2011]. Thus systematic long-term monitoring on a large spatial scale has been suggested to accurately assess the total CH4 emission from TGR drawdown areas.
 In this study, CH4 emissions were measured at four types of land (fallow land, cropland, deforested land, and rice paddies) in the drawdown area of TGR from November 2009 through January 2011. Our specific objectives were to (1) estimate the contribution of the drawdown area to total CH4 emissions from TGR, (2) assess the effect of land use on CH4 emissions in the drawdown areas, (3) analyze the spatiotemporal variations in CH4 emissions from different land types, and (4) determine any factors that may influence CH4 emission in the TGR drawdown area.
2. Methods and Materials
2.1. Site Description
 TGR is located within the watercourse of the Yangtze River, which has been flooded since 2003. The TGR is about 660 km in length, and has a surface area of 1084 km2, including the drawdown area of 450 km2. Water levels in TGR fluctuate seasonally by 30 m. The water level is held at 145 m during the flood season (June–August) to control flooding, which drains the drawdown area. The water level is gradually increased to 175 m after the flood season in order to increase the efficiency of electricity generation [Zhou et al., 2010]. The capacity to generate electricity at TGR was 18.2 million kW in 2010 (84.7 billion kWh of electricity were actually produced in 2010), making the TGR the largest hydroelectric producer in the world.
 The TGR is located in a subtropical monsoon climate zone with an annual mean temperature of 16.3–18.2°C and annual precipitation of 987–1326 mm [Guo et al., 2007]. Nearly 80% of the precipitation falls in the hot-wet season (April–September); only 20% falls in the cool-dry season (October–March) [Guo et al., 2007]. This study was carried out at three sites in the drawdown area near Zigui (30°51′N, 110°58′E), Wushan (31°03′N, 109°51′E), and Yunyang (30°56′N, 108°39′E), which are 2 km, 120 km and 240 km upstream from the Three Gorges Dam (Figure 1).
 Three kinds of plots (fallow land, cropland, and deforested land) at each site were selected in September 2009 when the plots were drained and the water level was below 146 m. A rice paddy (Oryza sativa), located at an elevation of 172 m in Yunyang, was added in June 2010 as a kind of agricultural wetland; thus making 10 experimental plots over 3 sites (Table 1). As lands below 160 m were frequently inundated by normal water level fluctuations or summer floods, only lands above 160 m were reclaimed for crop cultivation. Croplands were thus only located in the upper zone of the drawdown area at each of the three sites, while fallow and deforested lands were located in the lower zone, except for the deforested land in Wushan. Maize (Zea mays L.) was grown in the croplands of Zigui and Wushan, and sesame (Sesamum indicum L.) was grown in the cropland of Yunyang and the deforested land in Wushan. In the deforested lands, trees were cut down before the reservoir was impounded and many stumps were left on site.
Table 1. Elevation, Duration of Inundation, pH, and Soil Carbon and Nitrogen Levels at the Sampled Sitesa
Inundated Duration (d)
Organic C (g kg−1)
Total N (g kg−1)
The letters (a), (b), and (c) indicate significant difference (p < 0.05) at each site. Values are the mean ± SE (standard error). The average values of Yunyang do not include the values measured in the rice paddies.
6.42 ± 0.16(a)
10.72 ± 2.67(a)
0.78 ± 0.17(a)
6.64 ± 1.01(a)
11.18 ± 3.56(a)
0.90 ± 0.19(a)
6.21 ± 0.32(a)
11.44 ± 1.65(a)
0.85 ± 0.14(a)
6.42 ± 0.22
11.11 ± 0.36
0.81 ± 0.12
8.00 ± 0.20(a)
8.11 ± 1.13(a)
1.05 ± 0.10(a)
8.28 ± 0.08(a)
12.39 ± 2.43(b)
1.26 ± 0.24(b)
8.12 ± 0.10(a)
11.64 ± 2.69(b)
1.19 ± 0.20(a, b)
8.13 ± 0.14
10.71 ± 2.29
1.17 ± 0.11
8.29 ± 0.10(a)
4.68 ± 2.38(b)
0.57 ± 0.17(b)
8.63 ± 0.50(a)
2.66 ± 0.57(a)
0.34 ± 0.04(a)
8.25 ± 0.05(a)
3.55 ± 0.43(b)
0.48 ± 0.18(b)
8.39 ± 0.21
3.63 ± 1.01
0.46 ± 0.12
8.45 ± 0.26(a)
16.49 ± 2.47(c)
2.69 ± 0.83(c)
2.2. CH4 Emission Measurements
 CH4 emissions were measured using the static chamber method [Duchemin et al., 1995]. Two kinds of static chambers were deployed: 1) a floating static chamber for measuring CH4 emissions from the water surface, and 2) a closed static chamber was used for measuring CH4 emissions from dry land or rice paddies during the drained season. The same chambers were used for measuring CH4 emissions from dry lands both in the inundated and drained seasons. The floating static chamber (65 cm in length × 45 cm in width × 40 cm in height) consisted of a plastic box without a cover that was wrapped in light-reflecting and heatproof films to prevent temperature variation inside the chambers; in addition, plastic foam collars were fixed onto opposite sides of the chamber. The headspace height inside the chamber was about 30 cm. When the fallow lands, croplands, and deforested lands were drained, the above-described chambers were placed on permanently positioned aluminum bases (65 cm in length × 45 cm in width × 10 cm in height) with water grooves on top and inserted into the soil in order to ensure a tight fit at the air-soil interface. To avoid disturbing plant respiration and photosynthesis, any new growth grasses around the base were cleared before the gas samples were collected. A closed, static, steel frame chamber (50 cm in length × 50 cm in width × 75 cm in height for measuring emissions from rice paddies) was covered in polyethylene plastic film (85% transparent) and used to collect gas samples from rice paddy [Duan et al., 2005; Zheng et al., 2011a]. A silicone tube (0.6 cm and 0.4 cm outer and inner diameters, respectively) was inserted into the upper side of the chamber to collect gas samples and another silicone tube was inserted into the chamber to keep air pressure balanced between the inside and outside of the chamber. All measurements were performed in triplicate.
 In either flooded or drained seasons, the gases in the headspace of the chamber were collected into air-sampling bags (0.5 L; Hedetech, Dalian, China) five times every 10 min over a 40 min period using a hand-driven pump (ICQS-1; Beijing Municipal Institute of Labour Protection, Beijing, China). The gas samples were transported within 2–3 days after sampling to the State Key Laboratory of Urban and Regional Ecology (Beijing, China) for analysis using a gas chromatograph (Agilent 6820; Agilent Technologies, Santa Clara, USA) equipped with a flame ionization detector (FID) and separated with a Teflon column (2 m × 3 mm) packed with TDX-01(60/80 mesh). The oven, injector, and detector temperatures were 80°C, 150°C, and 300°C, respectively. The flow rate of the carrier gas (N2) was 30 mL min−1, and the flow rate of H2 and compressed air were set to 20 and 30 mL min−1, respectively. Standard CH4 gas (10.2 ppm in air; provided by China CH4 National Research Center for Certified Reference Materials, Beijing) was used to quantify the CH4 concentration in one of every 10 samples, which kept the coefficient of variation of the CH4 concentration in the replicated samples below 1%.
 We separated the diffusive and bubble emissions based on the change of CH4 concentration in the chambers. The CH4 emission was considered diffusive if the linear correlation between the CH4 concentration in the chamber and the elapsed time had r2 greater than 0.90 [Marani and Alvalá, 2007]. If the CH4 concentration was punctuated by one or more abrupt increases and the initial concentration in the chambers (at time t = 0) was close to the ambient air concentration, the abrupt increases were most easily explained by interception of rising gas bubbles by the chamber [Keller and Stallard, 1994]. The diffusive CH4 emission (Fd; mg CH4 m−2 h−1) was determined using
where ρ is the density of CH4 under standard conditions (0.714 kg m−3), dc/dt is the slope of the linear regression of the CH4 concentration in the chamber versus time, H is the height of the chamber above the water or soil surface (0.3 m for dry lands and 0.75 m for rice paddies), and T is the air temperature (°C).
 The bubble CH4 emission (Fb; mg CH4 m−2 h−1) was determined using
where ΔC is the gas concentration difference between the beginning and the end of the enclosure time in the chamber (ppm) and ΔT is the total time of emplacement (h).
 Cropland, deforested land, and fallow land were selected along one side of the Yangtze River at each site (Figure 1 and Table 1). The rice paddy plot was located at 4 km upstream of Yunyang (Figure 1). In each sampling plot, all measurements were conducted at the same places during all seasons, regardless of inundation or drainage. CH4 emissions were measured once or twice per month in the morning, weather depending, for 15 months (November 2009 to January 2011) in the fallow lands, croplands, deforested lands, and rice paddies at each growing stage and twice per month after the harvest. 17–21 times measurement was carried out at each land use of dry lands and 11 times at the rice paddy plot. CH4 emissions were measured from 8:00–18:00 at 2 h intervals about once every two months in the fallow land, cropland and deforested land in Zigui in order to assess the variability in CH4 emission during the daytime.
2.3. Environmental Variables
 During the inundated season, the following parameters were measured in situ: (1) velocity, using LS1206B, Midwest Group, Beijing, China; (2) pH, using HI 8424, Microcomputer HANNA, Rome, Italy; and (3) turbidity, using HI93703, Microcomputer HANNA. Air temperature, water temperature, and water depth were also measured in the field using alcohol thermometers and sounding ropes, respectively. In addition, water samples were collected once every month using plastic bottles (0.5 L) at a depth of 0.5 m and kept in a refrigerator at 4°C until laboratory analyses could be performed. Water quality parameters, including nitrate nitrogen (NO3−-N), ammonium nitrogen (NH4+-N), total nitrogen (TN), and total phosphorus (TP), were measured according to the methods of the State Environmental Protection Administration of China [Qi et al., 2002]. NO3−-N was determined by the spectrophotometric method with phenol disulfonic acid, and NH4+-N was determined by Nessler's reagent spectrophotometric method [Qi et al., 2002]. TN and TP were analyzed by peroxodisulfate oxidation of the original water samples. Total organic carbon (TOC) and total inorganic carbon (TIC) were detected using a total organic carbon analyzer (Liquic TOC; Elementar Co., Hanau, Germany). In the drained season, soil temperature was measured in the field using a waterproof thermometer (AD-5604; A&D Co., Tokyo, Japan) at a depth of 5 cm. Soil samples were collected once every month from a depth of 0–20 cm for laboratory analysis. Soil pH and organic carbon and total nitrogen levels were measured using a pH meter (Delta 320 pH meter; Mettler-Toledo Instruments Ltd., Shanghai, China) and elemental analyzer (Vario EL III; Elementar Co.), respectively.
2.4. Estimation of Total CH4 Emissions From the Drawdown Area
 To estimate the total CH4 emissions from the TGR drawdown area, two kinds of land (rice paddy and dryland, which included fallow land, cropland, and deforested land) and two periods (inundated and drained seasons) were studied. For each type of land use, the annual CH4 emission was calculated as the summation of the products of the CH4 emission rate, areas, and lengths of the inundated and drained season (equation (3)). Most of rice paddies were located in upland above the elevation of 170 m and inundated for 214 days with less variation (about 137 days as rice paddies in anaerobic condition, and 77 days as submerged drawdown areas). So the CH4 emission from all rice paddies was estimated with a constant inundation period. The total CH4 emission (TE) in the drawdown area was estimated by summing dryland and rice paddy emissions (equation (3)):
where i is the elevation; Pi is the inundated duration (days) for dryland at each elevation; FEin and FEdr are the CH4 emission rates of dryland during the inundated and drained seasons, respectively; Ai is the area of dryland at each elevation (range: 145–175 m) that was calculated from digital elevation model (DEM) data of the TGR drawdown area using ArcGIS 9.3 (ESRI Co., Redlands, USA); P′ is the inundated duration of the rice paddy; FEin′ and FEdr′ are the CH4 emission rates of the rice paddy during the inundated and drained seasons, respectively; and A0 is the total area of rice paddy, which accounted for 11% of the drawdown area [Ye et al., 2006].
2.5. Statistical Analysis
 One-way analysis of variance (ANOVA), in combination with the Tukey test, was used to analyze differences in soil pH, organic carbon, and total nitrogen levels between different land uses at the same site. The normal distribution of the CH4 emissions during the inundated and the drained seasons were tested using Kolmogorov-Smirnov Test. The skewed CH4 emissions distributions required the data set to be normalized by natural logarithmic transformation, and then differences between sites and land uses were tested using ANOVA. Two-way ANOVA was used to test interactions between sites and land uses in terms of CH4 emission during the inundated season. CH4 emissions were linearly regressed in terms of soil temperature at a depth of 5 cm, air-water temperature difference, air temperature, NH4+-N content and water depth. A multiple regression model was used to determine the key environmental variables that influenced CH4 emission during the inundated season. Data were analyzed with the SPSS 16.0 statistical package.
3.1. Water Level and Inundation Period
 The water level steadily decreased from a high of 171 m above sea level that was measured on 11 November 2009 (DOY315, 2009) when the study began (Figure 2). On 21 April 2010 (DOY111, 2010), the water level rose because of spring floods. From 9 May (DOY129, 2010), the water level was decreased to 145 m in order to control flooding (Figure 2). Two floods in the summer of 2010 caused short pulses in the water level on 19 July (DOY200, 2010) and 24 August (DOY236, 2010). On 29 August (DOY241, 2010), the water level began to rise until the target level of 175 m was achieved on 26 October (DOY299, 2010) (Figure 2).
 The inundated period for each plot varied according to its elevation and water level. All of the plots in the drawdown area were drained from 5 June (DOY156, 2010) through 22 August (DOY234, 2010), except for the short inundated period that were caused by floods (Figure 2). The croplands were inundated for less than 229 days above an elevation of 157 m in order to guarantee that the crops would ripen (Table 1).
3.2. Soil pH, Carbon, and Nitrogen During the Drainage Season
 The average soil pH in Zigui was 6.42, which was significantly lower than the pH of Wushan and Yunyang (8.13 and 8.39, respectively) (Table 1).The mean soil organic carbon content in Zigui was 11.11 g kg−1, which was similar to Wushan (10.71 g kg−1) but more than twice as high as Yunyang (3.63 g kg−1) (Table 1). The mean total nitrogen content in Zigui was 0.81 g kg−1, which was significantly lower than that of Wushan (1.17 g kg−1) but significantly higher than that of Yunyang (0.46 g kg−1) (Table 1).
 There were no significant differences in terms of soil pH among the different land uses at the same sites. For organic carbon and total nitrogen, there were no significant differences among the three types of lands used in Zigui, but organic carbon and total nitrogen levels were significantly lower in the fallow land of Wushan and the cropland of Yunyang compared with the other types of lands in Wushan and Yunyang, respectively (Table 1). Organic carbon and total nitrogen levels in the rice paddies were significantly higher than the levels measured in the other types of land studies in Yunyang (Table 1).
3.3. Water Velocity and Water Quality During the Inundated Season
 There were significant difference in terms of water velocity at all three sites, with the highest measured in Wushan (21.3 cm s−1) and the lowest in Zigui (5.2 cm s−1) (Table 2). Although the average turbidity was lower in Zigui (11.88 NTU) and Wushan (19.11 NTU) compared with Yunyang (33.71 NTU), the difference was not significant (Table 2). TP, TN, NH4+-N, NO3−-N, TIC, and TOC levels were not significantly different in the water samples collected at all three sites (Table 2).
Table 2. Water Velocity and Water Quality During the Inundated Season at the Zigui, Wushan, and Yunyang Sites of the Drawdown Area of the Three Gorges Reservoira
Vwater (cm s−1)
Total Phosphorus (mg L−1)
Total Nitrogen (mg L−1)
NH4+-N (mg L−1)
NO3−-N (mg L−1)
Total Inorganic Carbon (mg L−1)
Total Organic Carbon (mg L−1)
Values are the mean ± SE (standard error).
5.2 ± 3.9
11.88 ± 15.36
0.11 ± 0.12
1.54 ± 0.43
0.12 ± 0.11
1.37 ± 0.31
22.75 ± 4.21
1.67 ± 0.93
21.3 ± 14.6
19.11 ± 49.34
0.09 ± 0.04
1.28 ± 0.29
0.08 ± 0.05
1.11 ± 0.31
25.56 ± 3.29
2.00 ± 1.09
12.6 ± 8.5
33.71 ± 92.97
0.11 ± 0.04
1.58 ± 0.49
0.16 ± 0.13
1.26 ± 0.26
24.45 ± 3.05
1.68 ± 0.95
3.4. Diffusive CH4 Emissions From Different Land Uses and Sites
 The drawdown area was a source of CH4 during the inundated season, with emissions ranging from 0.10 to 0.37 mg CH4 m−2 h−1. The drawdown area acted as a sink or weak source of CH4 during the drained season, with emissions ranging from −0.034 to 0.036 mg CH4 m−2 h−1. The rice paddy, however, released 3.94 mg CH4 m−2 h−1 during the drained season (Table 3). No significant differences were present in terms of CH4 emission during the drained or the inundated seasons among the various land uses at the same sites, except the rice paddy (Table 3). Although there were no significant differences in CH4 emission between sites during the drained season, CH4 emissions in Wushan and Yunyang were significantly higher than those in Zigui for the same fallow lands, croplands, and deforested lands during the inundated season (Table 3).
Table 3. Average Diffusive CH4 Emissions of Different Land Types During the Drained and Inundated Seasons and the Entire Field Study (mg CH4 m−2 h−1)a
The letters (a), (b), and (c) indicate significant difference (p < 0.05) for each land use or average values at each site. Abbreviations: n, number of samples; SE, standard error.
Average CH4 emission of the fallow land, cropland, and deforested land at each site.
Total average CH4 emission of the fallow lands, croplands, and deforested lands at Zigui, Wushan, and Yunyang.
 The annual average CH4 emission from the croplands (0.12 mg CH4 m−2 h−1) was significantly lower than that of the fallows lands (0.19 mg CH4 m−2 h−1) and the deforested lands (0.18 mg CH4 m−2 h−1) (Table 3). The average CH4 emission across the entire sampled season was 2.61 mg CH4 m−2 h−1 in the rice paddy (Table 3), which was the highest among the four types of land that were examined. The average CH4 emission was the highest at Yunyang (0.24 mg CH4 m−2 h−1), followed by Wushan (0.15 mg CH4 m−2 h−1) and Zigui (0.10 mg CH4 m−2 h−1) (Table 3). There was a significant interaction between sites and land uses in terms of CH4 emissions during the inundated season.
3.5. Bubble CH4 Emission From the Drawdown Area
 During the inundated season, bubbles were observed 10 times in all the measurements, with a frequency of bubbles occurrence of 2.9% in the TGR drawdown area (Figure 3). The average bubble emission was 2.36 ± 2.15 mg CH4 m−2 h−1 when bubbles occurred, but the average bubble emission was 0.068 mg CH4 m−2 h−1 during the inundated season in consideration of the frequency of bubbles.
3.6. Variations in CH4 Emission During the Daytime
 CH4 emissions began to increase from 6:00 or 8:00 and reached maximum values at 12:00 or 14:00, then gradually decreased thereafter (Figure 4). The variations in CH4 emission during the daytime were small on most days, except in fallow lands on 11 March, croplands on 20 October, and deforested lands on 10 August and 30 May (Figure 4). In addition, the variations in CH4 emission during the daytime in croplands were less than those measured in fallow and deforested lands (Figure 4). Such 2 h measurement was not conducted at the rice paddy plot during the daytime.
 There were significant relationships between CH4 emission and water depth, air temperature, air-water temperature difference, and NH4+-N content during the inundated season and, additionally, soil temperature at a depth of 5 cm during the drained season (Figure 5). The results of the multiple regression analysis show that CH4 emission (F) is significantly related to the air-water temperature difference (T), water depth (D), and air temperature (Tair), as shown by equation (4):
3.8. Total CH4 Emission From the Drawdown Area of TGR
 In dryland, diffusive CH4 emission was estimated to be 233.9–490.3 Mg CH4 yr−1 during the inundated season and −22.4–21.6 Mg CH4 yr−1 during the drained season. Therefore, the annual diffusive CH4 emission was 211.5–511.9 Mg CH4 yr−1 in dry lands in the TGR drawdown area (Table 4). CH4 emission from rice paddies was estimated to be about 676.6 Mg CH4 yr−1 (Table 4). In addition, 145.4 Mg CH4 yr−1 was estimated from the drawdown area by bubbles (Table 4). Therefore, the total estimated CH4 emission from the TGR drawdown area was 1033.5–1333.9 Mg CH4 yr−1, which accounts for 42–54% of the CH4 emission from the water surface (2.46 Gg CH4 yr−1) [Chen et al., 2011].
Table 4. Estimation of CH4 Emission Levels From the Drawdown Area of the Three Gorges Reservoir
4.1. Contribution of the Drawdown Area to CH4 Emission in TGR
 Although hydropower, as a renewable source of energy, is considered an important way to mitigate global warming by replacing fossil fuel combustion for the generation of electricity, CH4 emissions from man-made hydropower reservoirs cause doubts regarding its mitigation potential when compared with traditional forms of fossil fuel energy [Cullenward and Victor, 2006]. Based on our monthly to semimonthly measurement on CH4 emissions from four types of land at three sites in the drawdown area along the mainstream of TGR, the annual average CH4 emission was 0.23 mg CH4 m−2 h−1 (0.16 mg CH4 m−2 h−1 of diffusive flux plus 0.068 mg CH4 m−2 h−1 of bubble flux) in the drawdown area of TGR in 2010 (Table 3), which is less than that reported by Chen et al.  (6.7 mg CH4 m−2 h−1), Chen et al.  (0.29 mg CH4 m−2 h−1), and Lu et al.  (0.34 mg CH4 m−2 h−1). Since the emission accounts for up to a half of the total emissions from the water surface, the drawdown areas of this reservoir should not be neglected when assessing emissions from hydropower reservoirs by potentially others.
4.2. Effect of Land Use on CH4 Emission
 The annual average CH4 emissions from croplands were smaller than those of the fallow and deforested lands most likely because the croplands were at higher elevation and inundated for a shorter period of time, which had a relatively short duration of anoxia. The annual average CH4 emissions from croplands, deforested lands, and fallow lands were positively related with their average durations of inundation (data not shown). Land use did not impact CH4 emissions at the same site during any season, except for rice paddies. Rice paddies, as a parcel of land that is waterlogged during the drained season, are a significant source of CH4 (Table 3). CH4 emissions from rice paddies have been measured for a long time in China because of their significant contribution to national CH4 emissions [Zhuang et al., 2009]. The average CH4 emission of Chinese rice paddies has been reported to be about 8.4 mg CH4 m−2 h−1 [Lu et al., 2010]. In this study, the average CH4 emission during the growing stage was 5.85 mg CH4 m−2 h−1.
4.3. Spatiotemporal Variations in CH4 Emission
 Seasonal variations in the water level affect the anaerobic conditions that ultimately determine CH4 emission. From June to August, the decline in the water level effectively drained all of the measured plots (Figure 2), except the rice paddy. In the drained season, CH4 emissions were weak, or the land acted as a weak sink because of the presence of methanotrophic bacteria under aerobic conditions. In this study during the drained period, the fallow lands, croplands, and deforested lands in Zigui and Wushan acted as CH4 sinks (−0.012 and −0.018 mg CH4 m−2 h−1, respectively), while small CH4 emissions were observed in Yunyang (0.011 mg CH4 m−2 h−1). Iqbal et al.  reported that vegetable fields, citrus orchards, and pine forests in Zigui act as CH4 sinks (−0.011 mg CH4 m−2 h−1). Compared with other reports on forest soil (−0.038 mg CH4 m−2 h−1) in Dinghushan Nature Reserve [Tang et al., 2006] and pine plantation and orchard soils (−0.029 mg CH4 m−2 h−1) in Heshan, Guangdong Province [Liu et al., 2008], the low CH4 uptake values in this study may be attributed to a higher soil pH (6.21–8.63 versus 3.9 in Dinghushan and 3.95–5.91 in Heshan), since acidic soil usually leads to a higher rate of CH4 uptake [Sitaula et al., 1995].
 When plots were inundated from September through the following February, CH4 was released from the water surface above the fallow lands, croplands, deforested lands, and rice paddies (Figure 2). CH4 emission from the TGR drawdown area was 0.22 mg CH4 m−2 h−1 during the inundated season, higher than that reported for the Ertan reservoir in southwest China (0.117 mg CH4 m−2 h−1) [Zheng et al., 2011b] and close to that reported for the Xiangxi tributary of TGR (0.2449 mg CH4 m−2 h−1) [Zhao et al., 2011]. In addition, our results are comparable to those reported for the boreal region of Canada, including the Laforge-1 (0.21 mg CH4 m−2 h−1) and La Grande-2 (0.58 mg CH4 m−2 h−1) [Duchemin et al., 1995] and 55 reservoirs nationwide distribution in Canada (0.37 ± 0.5 mg CH4 m−2 h−1) [Tremblay et al., 2005]. However, our results are remarkably lower than those reported for tropical reservoirs in Brazil (3.27 ± 2.75 mg CH4 m−2 h−1) [dos Santos et al., 2006] and Petit Saut Reservoir in French Guiana (1.93 ± 1.20 mg CH4 m−2 h−1) [Abril et al., 2005]. Barros et al.  found that CH4 emissions exponentially decline with increasing latitude, as the warm and anoxic conditions conducive to methanogenesis are less present in higher latitudes. This partly explains why TGR (29°16′–31°25′N) does not emit as much CH4 as tropical reservoirs. In addition, tropical reservoirs that were created by flooding uncleared tropical forests, such as Balbina in Brazil or Petit Saut Reservoir in French Guiana, are rich in organic carbon and able to contribute significantly more CH4 emissions. Intensive clearing before the impoundment of TGR did not provide much organic substrate for CH4 production.
 Water velocity and turbulence were important factors that contributed to the annual average CH4 emissions being highest upstream in Yunyang and decreasing gradually to Wushan and Zigui (Table 3). This spatial difference in CH4 emissions was apparent during the inundated season, but not during the drained season (Table 3), and was thus related to factors specific to water flow. Water velocity is an important source of turbulence at the air-water interface and influences the gas transfer velocity (k600), thereby enhancing CH4 emission from water surface [Borges et al., 2004; Ferrón et al., 2007]. Zigui, located 2 km upstream from the Three Gorges Dam, had significantly lower water velocity (5.2 cm s−1) than Wushan (21.3 cm s−1) and Yunyang (12.6 cm s−1) during the inundated season (p < 0.05) (Table 2). In addition, turbidity was higher upstream in Yunyang (33.71 NTU) than downstream in Wushan (19.11 NTU) and Zigui (11.88 NTU) during the inundated season (Table 2), potentially indicating that the greater sediment load upstream provided additional substrate for methanogenesis and thus emissions.
 Air temperature [Bergström et al., 2007], water temperature [Thérien and Morrison, 2005], and soil temperature [Juutinen et al., 2001] are important factors that influence the microbial activities that produce CH4 under anaerobic conditions. Increased difference of the air and water temperatures (Twater > Tair) might cause destabilization near the water surface, thereby enhancing the gas transfer velocity by as much as 4–30% due to evaporation [Guérin et al., 2007]. In this study, CH4 emission was influenced by the air-water temperature difference during the inundated season (Figure 5c), as has been seen elsewhere [Zheng et al., 2011b]. A regression analysis performed on the 2 h increment measurements at each site (data not shown) also revealed that air-water temperature difference accounted for 42.3% and 39.4% of CH4 emission variability at the fallow and deforested lands, respectively. During the drained season of this study, the soil temperature at a depth of 5 cm was positively correlated with CH4 emission (Figure 5e), which was in agreement with many other field studies [Iqbal et al., 2009; Liu et al., 2008]. Whether a soil was a net source or sink for CH4 depended on the relative rates between methanogenic and methanotrophic activities [Topp and Pattey, 1997], but methanogenic bacteria were much more responsive to temperature than methanotrophic bacteria, and optimum temperatures for both processes were about 25°C [Dunfield et al., 1993]. When temperature rose or fell, the CH4 production rate increased or decreased faster than that of CH4 consumption. Therefore, more CH4 was emitted at high temperatures and less CH4 was released at low temperatures.
 Due to seasonal fluctuations in the water level, the plots in the drawdown area switched from being a CH4 source (0.10–0.37 mg CH4 m−2 h−1) during the inundated season to being a weak source or sink (−0.034–0.036 mg CH4 m−2 h−1) during the drained season (Table 3). A similar transformation has been reported in alternating wet and dry zones in riverine zones and wetlands [e.g., Smith et al., 2000] and in a tundra ecosystem with areas of varying water saturation levels [e.g., Merbold et al., 2009]. CH4 is produced in soils as the end product of anaerobic organic matter decomposition [Topp and Pattey, 1997], and as exposed soils contain more oxygen than those overlain by water, higher emissions should happen when the drawdown areas are inundated. The negative relationship between CH4 emission and water depth found in this study and elsewhere [Soumis et al., 2004; Duchemin et al., 1995; Zheng et al., 2011b] is most likely due to the reduction in time for CH4 oxidation to occur with decreasing depths. Thus, more CH4 is able to reach the atmosphere [Juutinen et al., 2001]. Water depth was an important factor influencing hourly emission variations on different sampling days, as exemplified by the largest variation occurring on 11 March in the fallow lands when water depth was the shallowest (5 m). Methane emissions were also high on 10 August and 30 May in deforested lands partly because of shallow water depths.
 Land uses, especially rice cultivation and its management, are critical contributors to CH4 emission in the drawdown area of TGR. Among the other three land uses studied—fallow land, cropland, and deforested land—there was no significant difference in terms of CH4 emission during the drained and inundated seasons. Differences in annual average CH4 emissions are attributed to the periods of time that the measurement plots were inundated. Water level fluctuations were the main environmental factors that influenced CH4 emission. The average CH4 emissions decreased from upstream to downstream plots nearer to the drawdown area, which could be due to differences in water velocities and amounts of deposited sediment. The drawdown area occupies one third or more of the TGR surface area, and the total CH4 emission from the drawdown area is 42–54% of the total emissions from the reservoir surface. Ultimately, CH4 emissions from the drawdown areas of reservoirs require further study and consideration when assessing total seasonal emissions from such water bodies.
 This work was supported by the National Natural Science Foundation of China (50809067), Ministry of Science and Technology of the People's Republic of China (2010CB955904–03), and the Strategic Priority Research Program of the Chinese Academy of Sciences (XDA05060102 and XDA05050602). We also acknowledge Yafei Yuan for her suggestions on this article and three anonymous reviewers for their improvements to the paper.