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Journal of Changjiang River Scientific Research Institute >

2024 , Vol. 41 >Issue 9: 35 - 43

DOI: https://doi.org/10.11988/ckyyb.20230454

Water Environment and Water Ecology

Influence of Low-temperature Inflow on the Transport of Supersaturated Total Dissolved Gas in Deep-Water Reservoir

  • ZHOU Zhe-cheng , 1, 2, 3 ,
  • SHI Hao-yang 1, 2 ,
  • GUO Hui , 1, 2, 4 ,
  • WANG Zhi-xin 1, 2 ,
  • LI Xi-nan 5 ,
  • YANG Wen-jun 1, 2 ,
  • JIN Guang-qiu 3
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  • 1 Hydraulics Department,Changjiang River Scientific Research Institute,Wuhan 430010,China
  • 2 Hubei KeyLaboratory of Basin Water Resources and Eco-environmental Science, Changjiang River Scientific ResearchInstitute, Wuhan 430010, China
  • 3 College of Water Conservancy and Hydropower Engineering, HohaiUniversity, Nanjing 210098, China
  • 4 College of Environment, Hohai University, Nanjing 210098, China
  • 5 Department of Technological Innovation, Guizhou Survey & Design Research Institute for Water Resourcesand Hydropower, Guiyang 550002, China

Received date: 2023-05-04

  Revised date: 2023-08-21

  Online published: 2023-12-07

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Abstract

The stratification of water temperature in deep-water cascade reservoirs reduces the inflow temperature of downstream reservoir, altering the supersaturation degree of total dissolved gas (TDG) in flow discharges. With the Xiluodu-Xiangjiaba cascade reservoirs as a case study, we investigated the impact of lower-temperature inflow on the longitudinal and vertical transport processes of supersaturated TDG in deep-water reservoir via field observation in association with numerical simulation. Finds reveal that: 1) a 2 ℃ decrease in inflow temperature advances the submersion position of TDG cloud by 36.4 km, shifts the peak TDG saturation down by 55 m, and reduces its vertical influence range by 23%. 2) With a 2 ℃ decrease in inflow temperature, as the TDG cloud with a saturation over 110% transports to front of the Xiangjiaba dam, the decay rate of enveloped area decreases by 16%; in subsequent transport stage, the decay rate reduces by 44%. 3) The average longitudinal transport velocity of supersaturated TDG from the jet flow zone to the interflow zone plunges by 92%. (4) As inflow temperature reduces by 2 ℃, the peak and mean TDG saturation of the outflow from Xiangjiaba’s surface orifices reduce by 3.2 and 4 times that of the outflow from power generating set, respectively. (5) The compensation effect of temperature reduction on the safe water depth threshold for fish can be quantified as 0.20 m/ ℃. The findings provide scientific support for ecological dispatching of deep-water reservoirs during flood seasons.

Key words： TDG transport process; mathematical model; reservoir water temperature stratification; total dissolved gas; cloud position; water temperature compensation; ecological dispatching; cascade deep-water reservoir

Cite this article

ZHOU Zhe-cheng , SHI Hao-yang , GUO Hui , WANG Zhi-xin , LI Xi-nan , YANG Wen-jun , JIN Guang-qiu . Influence of Low-temperature Inflow on the Transport of Supersaturated Total Dissolved Gas in Deep-Water Reservoir[J]. Journal of Changjiang River Scientific Research Institute, 2024 , 41(9) : 35 -43 . DOI: 10.11988/ckyyb.20230454

0 引言

近年来,我国西南地区大型水电基地加速建设[1],有力支撑了国家双碳目标的实现,同时也产生了一定生态环境影响[2]。其中,大坝泄洪导致的水体总溶解气体(Total Dissolved Gas,TDG)过饱和现象会导致鱼类患上气泡病而死亡[3⇓-5]。早在20世纪60年代,TDG过饱和导致的鱼类死亡事件已在美国哥伦比亚流域梯级电站运行过程中被发现[6]。随着金沙江下游大量梯级高坝大库投入运行,TDG在深水库区中的输移过程变缓,累积效应增强[3],适应性生态调控需求显著。
输移过程中水体的TDG饱和度受水温、流速、水深、风速等因素影响[7-8],水温升高增大气体分子动能,TDG溶解度降低[5,9];流速增大加快水体垂向交换,TDG耗散速率增加;水深增加降低水体紊动,TDG耗散速率减缓[10-11];风速增大促进水气界面传质,TDG析出通量增加[12]。已有研究表明,梯级电站联合运行情景下,采用上游电站间隔泄洪,下游电站表孔泄洪的优化运行方式,可以缓解过饱和TDG对库区中鱼类的负面影响[13-14]。深水水库夏季水温分层现象显著[15],上游梯级来流水温的降低会导致深水库区水动力和水温结构的分布差异,进而影响水体溶解物质输移过程[16⇓-18],同样会对TDG在深水库区的输移过程产生影响。梯级水库低温来流对深水库区TDG输移过程的影响规律有待深入研究。
本文以溪洛渡—向家坝区间为研究区域,基于原位观测和数值模拟相结合的研究手段,从TDG输移过程、垂向分区模式、包络面积、迁移速度和对下游影响等方面,分析低温来流对深水水库TDG输移过程的影响规律,探讨水温和水深补偿效应对鱼类安全水深阈值的影响,研究成果可为深水水库生态调度提供科学支撑。

1 研究方法

1.1 研究区域

研究区域为溪洛渡-向家坝区间约156 km的库区江段,位于金沙江下游,地处四川省和云南省交界,如图1所示。溪洛渡水电站坝高285.5 m,为不完全年调节水库,调节库容64.6亿m3,设计洪峰流量43 700 m3/s[19]。向家坝水电站坝高161 m,为不完全季调节水库,调节库容9.03亿m3,设计洪峰流量41 200 m3/s[20]。向家坝电站下游自然河道为长江上游珍稀特有鱼类国家级保护区,鱼类资源丰富,根据以往调查核实,四川宜宾—向家坝河段的鱼类产卵场多达7处,珍稀特有鱼类的种类多达数十种,包括圆口鮦鱼、胭脂鱼、长吻鮠、达氏鲟等[21]。向家坝库区为山区狭长型河道水库[22],沿程流速随水深增加逐渐减小[23],5—7月份近坝区域会出现明显的水温分层现象,表底层最大温差达6.9 ℃[24-25]。
图1 研究区域示意图

Fig.1 Diagram of the study area

1.2 原位观测

本文采用2套原位观测数据,其中曾晨军等[26]在2017年6月获取的数据用于模型参数率定,项目组在2022年6月获取的数据用于模型验证。项目组的原位观测信息如图1和表1所示,由于项目组原位观测前溪洛渡持续泄洪,各监测断面水温垂向分布均一,TDG饱和度随水深增加而增大且垂向上的差异沿程扩大。
表1 原位观测断面信息

Table 1 Information of field observation cross-sections

断面
编号		 监测断面
名称		 坝下
距离/
km		 监测数据范围
测点水
深/m		 水温/℃ TDG饱和度/
%
1 溪洛渡电站
尾水出口		 1 — 19.4 134.0
2 永久大桥 3 2.0 19.5 127.1
3 洋丰码头 20 4.8 19.4 138.6
4 桧溪镇 33 [2.0,12.9] [19.3,19.5] [131.8,134.3]
5 南岸镇 80 [2.5,22.2] [19.4,19.7] [129.8,132.4]
6 向家坝坝前 150 [1.5,26.2] [19.3,19.4] [122.6,130.2]

1.3 数值模拟

1.3.1 数学模型

溪洛渡—向家坝区间是典型的山区狭长型水库[22],研究时段水温垂向分层现象明显,水温是影响TDG库区输移规律的关键因素之一。采用立面二维数学模型,将水体纵向划分为46个计算单元段,垂向划分为70层,每层层高2 m,控制方程如下:
连续性方程
∂ U B ∂ x + ∂ W B ∂ z = q B 　 。
动量方程
∂ U B ∂ t + ∂ U U B ∂ x + ∂ W U B ∂ z =
g B s i n α - B ρ ∂ P ∂ x + 1 ρ ∂ B τ x x ∂ x + 1 ρ ∂ B τ x z ∂ z 　 ,
1 ρ ∂ P ∂ z = g c o s α 　 。
自由水面方程
B η ∂ η ∂ t = ∂ ∂ x ∫ η h U B d z - ∫ η h q B d z 　 。
状态方程
ρ = f T w , Φ T D S , Φ I S S = ρ T + ρ s 　 。
输运方程
∂ Φ B ∂ t + ∂ U B Φ ∂ x + ∂ W B Φ ∂ z = ∂ B D x ∂ x 2 + ∂ B D z Φ ∂ z 2 + S Φ B 。
式中:U、W分别为纵向和垂向流速(m/s);q为单宽流量(m2/s);B为宽度(m);g为重力加速度(m/s2);α为河床与x轴方向的夹角(°);ρ为水体密度(kg/m3);τxx和τxz为紊动切应力(N/m2);P为压强(Pa);Bη为水面宽度(m);Tw为水温(℃);ΦTDS为总溶解固体浓度(mg/L);ΦISS为无机悬浮固体浓度(mg/L);h为水深(m);η为水面高程(m);ρT为水温影响下的水体密度(kg/m3);ρs为因水体内污染物所增加的水体密度(kg/m3);Φ为标量,代表溶解氧气浓度(mg/L)、溶解氮气浓度(mg/L)、TDG饱和度(%)或温度(℃);SΦ为标量所对应的源项;Dx为纵向弥散系数(m2/s);Dz为垂向弥散系数(m2/s)。

1.3.2 计算工况

分析已有研究成果,夏季水温分层期溪洛渡电站下泄水温约为20.2~22.2 ℃[27-28],在此水温范围内以0.4 ℃间隔,设置6个来流水温工况,各工况初始条件、来流边界条件均相同,以对比分析来流水温差异对深水库区过饱和TDG输移的影响。初始条件基于原位观测和已有研究成果[29]确定。气象条件设置为模拟区域夏季平均值。模型上游边界溪洛渡电站泄流流量和TDG饱和度过程见图2(a),模型下游边界向家坝电站不同泄流方式的流量过程见图2(b)。
图2 上游和下游边界条件

注:图2(a)中的TDG饱和度为研究时段平均来流水温21.8 ℃工况下的饱和度,各来流水温工况下上游来流的溶解氧气浓度和氮气浓度相同。

Fig.2 Upstream and downstream boundary conditions

1.3.3 率定与验证

采用平均绝对误差(Mean Absolute Error,MAE)和均方根误差(Root Mean Squared Error,RMSE)评价模型率定和验证结果,其计算式分别为
M A E = ∑ i = 1 n X o b s , i - X m o d e l , i n 　 ;
R M S E = ∑ i = 1 n X o b s , i - X m o d e l , i 2 n 　 。
式中:Xobs,i表示实测值;Xmodel,i表示模拟值。
采用2017年6月20日至2017年7月3日间的断面水位、水温和TDG饱和度实测数据[26]对模型敏感参数进行率定,结果如图3—图5所示,模拟结果可较好地表征水位、水温和TDG饱和度的空间分布,水位和水温的MAE和RMSE均不到实测值的0.5%,TDG饱和度的MAE和RMSE均不到实测值1.5%,误差在合理范围内。
图3 向家坝坝前断面水位率定结果

Fig.3 Calibration result of water level at cross-section in front of Xiangjiaba dam

图4 水温垂向分布率定结果

Fig.4 Calibration result of vertical water temperature distribution

图5 不同深度下TDG饱和度纵向沿程分布率定结果

Fig.5 Calibration result of longitudinal distribution of TDG saturation at different depths

采用2022年6月24—28日实测的水温、TDG饱和度进行模型验证,各断面水温、TDG饱和度的实测值与模拟值基本一致,模型能较好地反映水温和TDG饱和度的垂向结构。结果如图6所示。
图6 水温和TDG饱和度垂向分布验证结果

Fig.6 Validation results of vertical distribution of water temperature and TDG saturation

1.4 补偿效应分析

鱼类对TDG饱和度的实际感知程度受所处位置的水温和水深补偿作用影响,通常将补偿校正后的TDG饱和度临界值(110%)作为鱼类安全阈值[30⇓⇓-33]。
TDG饱和度的深度补偿效应可通过式(9)计算。
G c o m p = P T D G P a l t + ρ g h / 1000 × 100 % 　 。
式中:Gcomp为深度补偿后TDG饱和度(%);PTDG为水深h处总溶解气体压力(kPa);Palt为当地大气压力(kPa);ρ为水的密度(kg/m3);h为鱼类所在水深(m)。
考虑水温差异对水体溶解氧气和溶解氮气浓度的影响,TDG饱和度的水温补偿效应可通过下式计算,即
T D G = 0.79 Φ O 2 Φ O 2 s a t + 0.21 Φ N 2 Φ N 2 s a t × 100 % 　 。
式中:TDG为总溶解气体饱和度(%); Φ O 2为水体中氧气浓度(mg/L); Φ O 2 s a t为水体对应水温下的氧气饱和浓度(mg/L); Φ N 2为水体中氮气浓度(mg/L); Φ N 2 s a t为水体对应水温下的氮气饱和浓度(mg/L)。

2 结果与讨论

2.1 低温来流对深水水库过饱和TDG输移过程的影响

水库温度分层密度流纵向沿程可分为射流区、下潜区和交换区[34],输移至交换区的过饱和TDG会呈现垂向分层现象,该饱和度垂向分层区可划分为上层低饱和度区(100%<饱和度<105%)、中层高饱和度区(105%<饱和度)、底层欠饱和区(饱和度<100%),如图7所示。
图7 溪洛渡—向家坝区间过饱和TDG分区模式

注:S=150 km处于向家坝坝前,计算区域为国家坝库区沿河道中心线的纵剖面,以下同。

Fig.7 Zoning of supersaturated TDG in Xiluodu-Xiangjiaba cascade reservoirs

不同来流水温条件下TDG在库区中的时空输移过程如图8所示,过饱和TDG在溪洛渡—向家坝区间呈云团状输移,泄洪后第3天开始逐步潜入饱和度垂向分层区,第6天左右云团前锋抵达向家坝坝前,最终部分过饱和TDG随表孔和机组出流排放至下游,剩余过饱和TDG在回水区域通过传质作用和沉积物耗氧而耗散。随着来流水温降低,过饱和TDG输移路径呈现向底层移动的趋势。
图8 温度补偿下不同来流温度工况过饱和TDG在库区的输移过程

Fig.8 Transport processes of supersaturated TDG clouds with different inflow temperatures under temperature compensation effect

从高饱和度TDG云团潜入位置变化看,泄洪后第3天,潜入位置随来流水温降低而提前,提前量与来流水温降低量呈显著线性关系(y=-0.91+18.07x,R2=0.99,式中x为来流水温较22.2 ℃的降低量(℃),y为潜入位置较来流水温22.2 ℃工况的提前量(km))。潜入位置由来流水温22.2 ℃工况的坝下约113.4 km提前至来流水温20.2 ℃工况的坝下约77.0 km,提前36.4 km。
从高饱和度TDG云团(饱和度>130%)垂向位置变化看,泄洪后第6天,TDG云团完全潜入交换区且尚未下泄,TDG峰值垂向位置随来流水温降低而下移,下移量与来流水温降低量呈显著对数关系(y=41.11+18ln(x+0.154),R2=0.99,式中x为来流水温较22.2 ℃的降低量(℃),y为TDG峰值垂向位置较来流水温22.2 ℃工况的下移量(m)),TDG峰值垂向位置由来流水温22.2 ℃工况的338 m下移至来流水温20.2 ℃工况的283 m,下移55 m。云团垂向影响范围随来流水温降低而减小,垂向水深影响范围与最大水深的比值由来流水温22.2 ℃工况的0.82降至来流水温20.2 ℃工况的0.63。输移路径的变化改变了过饱和TDG的垂向分布模式,进而影响过饱和TDG的释放过程。

2.2 低温来流对深水水库高饱和度TDG云团衰减的影响

高饱和度TDG云团衰减速率可以用单位时间内特定TDG饱和度等值线的包络面积占比变化量来表征,即包络面积衰减速率,来流水温20.2 ℃和22.2 ℃两个工况下不同TDG饱和度等值线包络面积占比随时间的变化如图9所示。以TDG饱和度为110%的等值线包络面积占比为例,高饱和度TDG云团输移至向家坝坝前阶段,即泄洪后第4天至第6天,随来流水温降低,过饱和TDG云团垂向位置下移(见图8),水体水温低承压大,减少了溶解气体分子动能,阻碍了水气传质作用[9-10,12],包络面积衰减速率降低。来流水温22.2 ℃工况下,包络面积占比由75.5%降至50.3%,包络面积衰减速率为12.6%/d(见图9(b));来流水温20.2 ℃工况下,包络面积占比由79.6%降至58.3%,包络面积衰减速率降至10.6%/d(见图9(a)),较来流水温22.2 ℃工况下降16%。
图9 TDG饱和度面积百分比累积曲线

Fig.9 Accumulated curves of the percentage of TDG saturation area

高饱和度TDG云团往向家坝下游输移阶段,即泄洪后第6天至第8天,水气传质作用随大气和水体间TDG浓度差的减小而减弱,随着来流水温的升高,过饱和TDG云团垂向上逐渐靠近向家坝表孔和机组出流位置,随水流下泄而减小的高饱和度TDG云团面积大于水气传质作用减小的面积。本阶段包络面积的衰减速率同样呈现出随来流水温降低而减小的趋势,但衰减速率与上一阶段的差异随来流水温的降低而增大,来流水温22.2 ℃工况下,包络面积占比由50.3%降低至25.6%,包络面积衰减速率为12.4%/d,较上一阶段略有降低。来流水温20.2 ℃工况下,包络面积占比由58.3%降低至44.4%,包络面积衰减速率为7.0%/d,较来流水温22.2 ℃工况下降44%,较上一阶段下降34%。

2.3 低温来流对深水水库过饱和TDG纵向迁移速度的影响

过饱和TDG的纵向迁移速度可以用单位时间内特定TDG饱和度等值线前锋的平均纵向位置变化量来表征,TDG饱和度为130%的等值线前锋平均纵向位置随时间的变化过程如图10所示。TDG纵向迁移速度可以划分为3个逐步降低的演变阶段。①射流区快速迁移阶段:泄洪后6 h内,在大坝泄流初始动量的影响下纵向迁移速度较快,过饱和TDG平均纵向迁移速度约为6.08 km/h。②下潜区减速迁移阶段:泄洪后6 h至泄洪后第3天,高饱和度TDG逐渐从射流区进入到下潜区,由于水深增加负浮力作用增大,过饱和TDG垂向迁移速度增加纵向迁移速度减小,平均纵向迁移速度大幅下降至1.26 km/h,较射流区快速迁移阶段下降79%。③交换区缓慢迁移阶段:泄洪3 d以后,过饱和TDG基本潜入水下,纵向迁移速度进一步下降至0.48 km/h,较射流区快速迁移阶段下降92%。
图10 饱和度前锋平均纵向位置随时间的变化(饱和度=130%)

Fig.10 Time-dependent change in mean longitudinal position of saturation front (saturation degree 130%)

TDG纵向迁移速度受来流水温变化影响,如图11所示,泄洪后前3 d,过饱和TDG主要在射流区和下潜区输移,来流水温越低,所受负浮力作用越大,TDG纵向迁移速度降低,前锋位置随着来流水温降低而延后;泄洪后第4天至泄洪后第6天,过饱和TDG从下潜区逐步进入交换区,来流水温越低,TDG云团的垂向位置越靠近底部,TDG纵向迁移速度先减小后增大,TDG云团前锋位置随着来流水温的降低先延后再提前,这与水槽实验得出的研究结果相符合[35⇓-37],即密度流沿着水体顶部和底部输移时的速度大,沿着分层水体中间输移时速度小。
图11 饱和度前锋平均纵向位置距平随时间的变化(饱和度=130%)

Fig.11 Time-dependent change in the anomaly of mean longitudinal position of saturation front (saturation degree 130%)

2.4 低温来流对下游电站出流过饱和TDG强度的影响

向家坝表孔和机组出流水体TDG饱和度随时间的变化如图12所示。从泄流水体的TDG饱和度峰值和均值大小看,表孔和机组出流水体饱和度的峰值和均值随着来流水温的降低呈现减小趋势,当来流水温由22.2 ℃逐步降低至20.2 ℃时,表孔出流水体饱和度的峰值和均值分别下降17%和9%;机组出流水体饱和度的峰值和均值分别下降5%和3%。从泄流水体TDG饱和度峰值出现时间看,随着来流水温由22.2 ℃逐步降低至20.2 ℃,表孔出流水体饱和度峰值出现时间呈现提前趋势,机组出流水体饱和度峰值出现时间呈现先延后再提前的趋势。从高TDG饱和度水体(饱和度>120%)的下泄持续时间来看,随着来流水温由22.2 ℃逐步降低至20.2 ℃,表孔出流的下泄持续时间呈现缩短趋势,持续时间从89.76 h逐步缩短至0 h;机组过流的下泄持续时间呈现稍延长后显著缩短的趋势,持续时间逐步从98.02 h延长至99.40 h再显著缩短至62.48 h。
图12 表孔和机组出流水体TDG饱和度随时间的变化

Fig.12 Time-dependent variations of the saturation degrees of TDG in the outflow from surface orifices and power generating sets

来流水温降低导致高饱和度TDG云团垂向位置下移,垂向影响范围减小,相同深度下TDG饱和度纵向上分布差异减小,出流水体的TDG饱和度随时间的分布逐渐扁平化,表孔出流由于出口高程高,仅在云团垂向位置下移之前才会出现明显TDG峰值,因此来流水温越低的工况TDG峰值出现时间越早;机组过流水体由于出口高程低,在高饱和度TDG云团下移之后仍在云团影响范围,过饱和TDG的纵向迁移速度是决定TDG峰值出现时间以及高饱和度水体下泄持续时间的关键因素。

2.5 水温和水深补偿对鱼类安全水深阈值的影响

TDG在液相中的平衡浓度与其在气相中的分压成正比,与温度负相关[38],鱼类安全水深的精准确定需要在深度补偿[26]基础上考虑温度补偿的作用,尤其是对于溪洛渡坝下近区和向家坝下游自然河道这类水深浅且水温受上游泄流影响大的水体,鱼类回避高饱和度TDG所能利用的深度补偿有限,温度补偿对于自然河道中鱼类安全水深确定有一定影响。如图13所示,考虑深度补偿后TDG饱和度随着水深的增加急剧下降,叠加温度补偿之后,饱和度在深度补偿的基础上进一步减少且水温越低减小程度越大。参考美国、加拿大等国的标准及以往鱼类耐受性成果[30⇓⇓-33],将TDG饱和度<110%的区域作为鱼类的安全区域,补偿效应下鱼类安全水深阈值如表2所示,水体TDG饱和度分别为140%、130%和120%条件下,安全水深阈值均随着水温降低而线性减小,水温降低对安全水深阈值的补偿效应可量化为0.20 m/℃。
图13 温度补偿和深度补偿对于水体TDG饱和度的影响

注:TDG饱和度140%指来流水温21.8 ℃工况下水体的TDG饱和度(未进行分层取水调控时,研究时段向家坝水库平均来流水温为21.8 ℃,因此以21.8 ℃为基准),特定饱和度下各来流水温工况的氧气浓度和氮气浓度相同。

Fig.13 Effect of temperature compensation and depth compensation on TDG saturation

表2 补偿效应下不同饱和度的鱼类安全水深阈值(当地大气压为96.84 kPa时)

Table 2 Safe water depth thresholds for fish at different TDG saturation levels under compensation effects at local atmospheric pressure of 96.84 kPa

坝下近区
TDG饱和
度/%		 不同水温下的安全水深阈值/m
22.2 ℃ 21.8 ℃ 21.4 ℃ 21.0 ℃ 20.6 ℃ 20.2 ℃
140 2.48 2.42 2.30 2.24 2.13 2.06
130 1.60 1.53 1.43 1.36 1.27 1.20
120 0.71 0.64 0.56 0.49 0.41 0.34

3 结论

(1)来流水温显著影响过饱和TDG在深水库区中的纵向和垂向输移过程。高饱和度TDG云团潜入时的纵向位置随着来流水温的降低呈现线性函数趋势提前,峰值垂向位置随来流水温的降低呈现对数函数趋势下移。
(2)来流水温降低会减小高饱和度TDG云团在库区内的衰减速率,但不同输移阶段的影响程度存在较大差异,高饱和度TDG云团输移至向家坝坝前阶段和往向家坝下游输移阶段的包络面积衰减速率的差异随来流水温的降低而增大。
(3)深水水库过饱和TDG的纵向迁移过程可划分为射流区快速迁移、下潜区减速迁移和交换区缓慢迁移3个阶段,平均纵向迁移速度在3个阶段内呈现显著降低和持续降低的变化规律。随来流水温的降低,TDG纵向迁移速度在射流区和下潜区内随来流水温的降低而减少,在交换区内随来流水温的降低先减小后增加。
(4)下游电站表孔和机组出流饱和度峰值、均值以及高饱和度泄流持续时间随着上游来流水温的降低呈现减小趋势,表孔减小程度更显著,泄洪前后短期低温水下泄可降低高饱和度TDG对下游自然河道水体的影响。
(5)在深度补偿基础上耦合温度补偿后,鱼类安全水深阈值均随着水温降低而线性减小,水温降低对安全水深阈值的补偿效应可量化为0.20 m/℃,温度补偿对于自然河道中鱼类安全水深确定有一定影响。

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