大渡河流域面雨量时空分布特征及雨季转换指标
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摘要
利用1961—2016年大渡河流域15个气象站逐日降水资料,采用算术平均法计算上、中、下游三个分段流域的面雨量,对其时空分布特征进行分析,计算流域内雨季开始及结束期。结果表明:(1)大渡河中、上游面雨量呈上升趋势,下游呈下降趋势,下游年降水量相对变率和极差最大,其次是中游,上游最小;夏季流域面雨量最大,占全年降水的50%～60%。5—9月流域面雨量在100～200 mm之间,11月至翌年2月在5～20 mm之间,流域内面雨量峰值出现时间由北向南延迟,上、中、下游相差近1个月。(2)依据雨季转换指标计算出的雨季开始及结束期比依据强降水计算的更稳定,大渡河流域下游进入雨季最早,其次是中游,上游最晚,而上游雨季结束最早,其次是中游,下游最晚,上、中、下游雨季持续时间分别为172 d、182 d和195 d。(3)当上游出现强降水时,中、下游很少同时出现强降水,当下游出现强降水时,中游经常同时也出现强降水。
Based on the daily precipitation data of 15 meteorological stations in the Dadu River Basin during 1961-2016, the areal precipitation of the upper, middle and lower reaches of the Dadu River Basin was caculated by using arithmetic average method. And the spatial and temporal distribution characteristics of its areal precipitation were analyzed. In addition, the beginning and ending date of the rainy season in the Dadu River Basin were calculated in this article. The results are as follows:(1) The areal precipitation of the middle and upper reaches of the Dadu River Basin showed an upward trend, while that of the lower reaches showed a downward trend. The relative variability and range of annual precipitation in the lower reaches were the largest, followed by the middle and the upper reaches. The areal rainfall was maximum in the Dadu River Basin in summer, it was about 50%-60% of the annual precipitation. The monthly average areal rainfall in the Dadu River Basin was 100-200 mm from May to September, and 5-20 mm from November to the following February. The peak of areal rainfall in the Dadu River Basin from north to south was delayed about a month.(2) The beginning and ending period of the rainy season calculated by the conversion index of the rainy season was more stable than that calculated by the heavy rainfall. The lower reaches of the Dadu River Basin entered the rainy season at the earliest, followed by the middle and the upper reaches. The upper reaches of the Dadu River Basin ended the rainy season at the earliest, followed by the middle and the lower reaches. The duration of rainy season in the upper, middle and lower reaches were 172 days, 182 days and 195 days, respectively.(3) Under the condition of heavy precipitation occurring in the upper reaches of the Dadu River Basin, the probability of heavy precipitation occurring in the middle and lower reaches at the same time was very small. Nevertheless, the heavy precipitation often occurred in the middle reaches of the Dadu River Basin at the same time when heavy precipitation occurred in the lower reaches.
Based on the daily precipitation data of 15 meteorological stations in the Dadu River Basin during 1961-2016, the areal precipitation of the upper, middle and lower reaches of the Dadu River Basin was caculated by using arithmetic average method. And the spatial and temporal distribution characteristics of its areal precipitation were analyzed. In addition, the beginning and ending date of the rainy season in the Dadu River Basin were calculated in this article. The results are as follows:(1) The areal precipitation of the middle and upper reaches of the Dadu River Basin showed an upward trend, while that of the lower reaches showed a downward trend. The relative variability and range of annual precipitation in the lower reaches were the largest, followed by the middle and the upper reaches. The areal rainfall was maximum in the Dadu River Basin in summer, it was about 50%-60% of the annual precipitation. The monthly average areal rainfall in the Dadu River Basin was 100-200 mm from May to September, and 5-20 mm from November to the following February. The peak of areal rainfall in the Dadu River Basin from north to south was delayed about a month.(2) The beginning and ending period of the rainy season calculated by the conversion index of the rainy season was more stable than that calculated by the heavy rainfall. The lower reaches of the Dadu River Basin entered the rainy season at the earliest, followed by the middle and the upper reaches. The upper reaches of the Dadu River Basin ended the rainy season at the earliest, followed by the middle and the lower reaches. The duration of rainy season in the upper, middle and lower reaches were 172 days, 182 days and 195 days, respectively.(3) Under the condition of heavy precipitation occurring in the upper reaches of the Dadu River Basin, the probability of heavy precipitation occurring in the middle and lower reaches at the same time was very small. Nevertheless, the heavy precipitation often occurred in the middle reaches of the Dadu River Basin at the same time when heavy precipitation occurred in the lower reaches.
引文
[1] 高琦,徐明,李武阶,等.长江上游六流域强降水面雨量特征分析[J].人民长江,2013,44(13):14 -17.
[2] 李武阶,王仁乔,郑启松.几种面雨量计算方法在气象和水文上的应用比较[J].暴雨灾害,2000(1):62-67.
[3] 陈宁,黄鹂,沈树勤,等.江苏省流域面雨量气候特征及雨涝关系的探讨[J].气象科学,2005,25(5):518-527.
[4] 徐晶,姚学祥.流域面雨量估算技术综述[J].气象,2007,33(7):15-21.
[5] 吴璐,靖春悦,张晓鹏,等.沙澧河上游关键区汛期强降水面雨量对洪峰的影响[J].气象与环境科学,2010,33(3):29-32.
[6] 朱占云,潘娅英,骆月珍,等.浙江省水库流域面雨量的多模式预报效果分析与检验[J].气象与环境科学,2017,40(3):93-100.
[7] 江清霞.基于GIS的沙澧河流域面雨量算法对比分析[J].气象与环境科学,2014,37(2):94-99.
[8] 叶正伟,李宗花.1951年来洪泽湖流域面雨量变化特征与趋势分析[J].长江流域资源与环境,2010,19(12):1392-1396.
[9] 卢珊,王百朋,贺皓,等.汉江上游汛期面雨量气候特征[J].干旱气象,2014,32(2):201-206.
[10] 常军,史恒斌,左璇.黄河流域秋季降水及环流对ENSO和IOD的响应分析[J].气象与环境科学,2013,36(2):15-20.
[11] 李林,扎西央宗,卓玛,等.西藏年楚河流域冰川及冰川湖变化特征及其对气候变化的响应[J].高原山地气象研究,2018,(2):28-34.
[12] 刘倪,叶金印.淮河流域汛期暴雨与西太平洋海温关系[J].沙漠与绿洲气象,2014,8(5):39-43.
[13] 黄玖珺.车尔臣河流域1955—2010年气候变化特征分析[J].沙漠与绿洲气象,2012,6(6):28-33.
[14] 陈宏,尉英华,王颖,等.基于VIC水文模型的滦河流域径流变化特征及其影响因素[J].干旱气象,2017,35(5):776-783.
[15] 康晓燕,马学谦,韩辉邦,等.1981—2015年黄河上游河曲地区大气可降水量变化特征[J].干旱气象,2017,35(6):975-983.
[16] 刘承晓,张蕾.江淮流域春季可利用降水量变化特征[J].干旱气象,2016,34(6):976-982.
[17] 朱丽,刘蓉,文军,等.近50 a来洮河流域气候变化和干旱演变过程[J].干旱气象,2018,36(2):234-242.
[18] 李武阶,王继竹,郭英莲,等.金沙江中下游流域面雨量特征分析[J].长江流域资源与环境,2014,23(6):846-853.
[19] 钟利华,李勇,李仲怡,等.近45 a西江流域汛期暴雨面雨量时空分布特征[J].暴雨灾害,2018,37(1):24-31.
[20] 王仁乔,李才媛,王丽,等.六大流域强降水面雨量气候特征分析[J].气象,2003,29(7):38-42.
[21] 程珂,周东升,李铭,等.大渡河流域近51年降水径流特征分析[J].水电能源科学,2013,31(2):5-8.
[22] 吴付华,樊明兰,程琳.大渡河干流暴雨洪水特性初步分析[J].四川水力发电,2013,32(1):4-7.
[23] 刘佳,马振峰,杨淑群,等.1961—2010年大渡河流域极端降水事件变化特征[J].长江流域资源与环境,2015,24(12):2166-2176.
[24] 宋雯雯,郭洁.大渡河流域积雪特征及其与气候要素和径流的关系[J].高原山地气象研究,2017,37(2):45-49.
[25] 于大峰,陈良华,孙士型,等.长江上游流域面雨量时空分布特征[J].干旱气象,2012,30(4):563-569.
[2] 李武阶,王仁乔,郑启松.几种面雨量计算方法在气象和水文上的应用比较[J].暴雨灾害,2000(1):62-67.
[3] 陈宁,黄鹂,沈树勤,等.江苏省流域面雨量气候特征及雨涝关系的探讨[J].气象科学,2005,25(5):518-527.
[4] 徐晶,姚学祥.流域面雨量估算技术综述[J].气象,2007,33(7):15-21.
[5] 吴璐,靖春悦,张晓鹏,等.沙澧河上游关键区汛期强降水面雨量对洪峰的影响[J].气象与环境科学,2010,33(3):29-32.
[6] 朱占云,潘娅英,骆月珍,等.浙江省水库流域面雨量的多模式预报效果分析与检验[J].气象与环境科学,2017,40(3):93-100.
[7] 江清霞.基于GIS的沙澧河流域面雨量算法对比分析[J].气象与环境科学,2014,37(2):94-99.
[8] 叶正伟,李宗花.1951年来洪泽湖流域面雨量变化特征与趋势分析[J].长江流域资源与环境,2010,19(12):1392-1396.
[9] 卢珊,王百朋,贺皓,等.汉江上游汛期面雨量气候特征[J].干旱气象,2014,32(2):201-206.
[10] 常军,史恒斌,左璇.黄河流域秋季降水及环流对ENSO和IOD的响应分析[J].气象与环境科学,2013,36(2):15-20.
[11] 李林,扎西央宗,卓玛,等.西藏年楚河流域冰川及冰川湖变化特征及其对气候变化的响应[J].高原山地气象研究,2018,(2):28-34.
[12] 刘倪,叶金印.淮河流域汛期暴雨与西太平洋海温关系[J].沙漠与绿洲气象,2014,8(5):39-43.
[13] 黄玖珺.车尔臣河流域1955—2010年气候变化特征分析[J].沙漠与绿洲气象,2012,6(6):28-33.
[14] 陈宏,尉英华,王颖,等.基于VIC水文模型的滦河流域径流变化特征及其影响因素[J].干旱气象,2017,35(5):776-783.
[15] 康晓燕,马学谦,韩辉邦,等.1981—2015年黄河上游河曲地区大气可降水量变化特征[J].干旱气象,2017,35(6):975-983.
[16] 刘承晓,张蕾.江淮流域春季可利用降水量变化特征[J].干旱气象,2016,34(6):976-982.
[17] 朱丽,刘蓉,文军,等.近50 a来洮河流域气候变化和干旱演变过程[J].干旱气象,2018,36(2):234-242.
[18] 李武阶,王继竹,郭英莲,等.金沙江中下游流域面雨量特征分析[J].长江流域资源与环境,2014,23(6):846-853.
[19] 钟利华,李勇,李仲怡,等.近45 a西江流域汛期暴雨面雨量时空分布特征[J].暴雨灾害,2018,37(1):24-31.
[20] 王仁乔,李才媛,王丽,等.六大流域强降水面雨量气候特征分析[J].气象,2003,29(7):38-42.
[21] 程珂,周东升,李铭,等.大渡河流域近51年降水径流特征分析[J].水电能源科学,2013,31(2):5-8.
[22] 吴付华,樊明兰,程琳.大渡河干流暴雨洪水特性初步分析[J].四川水力发电,2013,32(1):4-7.
[23] 刘佳,马振峰,杨淑群,等.1961—2010年大渡河流域极端降水事件变化特征[J].长江流域资源与环境,2015,24(12):2166-2176.
[24] 宋雯雯,郭洁.大渡河流域积雪特征及其与气候要素和径流的关系[J].高原山地气象研究,2017,37(2):45-49.
[25] 于大峰,陈良华,孙士型,等.长江上游流域面雨量时空分布特征[J].干旱气象,2012,30(4):563-569.