黄河中上游季节内强降水的时间非均匀性特征及其对大气环流的响应

doi:10.7522/j.issn.1000-694X.2013.00033

摘要/Abstract

摘要：

应用1960—2008年5—10月黄河中上游流域66个气象台站降水资料和美国环境预测中心及大气研究中心（NCEP/NCAR）再分析资料，综合气候分区及地表水系分布情况，将黄河中上游流域分为高原区、干旱区、季风影响区，以强降水集中度（SCD）和强降水集中期（SCP）来表征强降水的非均匀性特征，并对SCP异常年份的强降水的变化特征及环流形式进行分析。结果表明：①黄河中上游流域大部分地区强降水依赖化的特征显著，强降水分布最为均匀的地区为秦岭北麓及山西南部，降水最为集中的地区为河套地区及陕北等地。②在黄河中上游流域，3个区强降水平均发生的时间先后顺序为季风影响区最晚、干旱区次之、高原区最早，且均相差一候；黄河流域季风影响区的南部渭河、泾河、洛河等处及青藏高原东部的兰州附近为大的SCP变率区，强降水发生的时间变动较大，鄂尔多斯高原东北部为小的SCP变率区，强降水发生时间稳定；干旱区与季风影响区汛期SCP于20世纪90年代初期发生由大变小的显著性突变，且干旱区突变提前于季风影响区。③干旱区汛期SCP异常年份的高空环流显示，当西太平洋副高北抬至30°N以北120°E左右、南亚高压维持在30°N左右120°E以东时，若两高压“同进同退”(“同向而进、背向而退”)，则强降水发生在汛期(7月中旬—8月下旬)后(前)期。黄河流域季风影响区强降水异常年份的高空环流显示，当西太平洋副热带高压维持在26°—30°N、120°E左右，南亚高压维持在30°N左右、120°E以西时，若两高压“同进同退”(“同向而进、背向而退”)，则强降水发生在汛期后(前)期。

关键词: 黄河中上游流域, 强降水集中期(SCP), 强降水集中度(SCD), 季节内非均匀性特征, 大气环流

Abstract:

Based on the daily precipitation data collected in May through October during 1960-2008 and the NCAR/NCEP reanalysis data, we analyzed the characteristics of the rainfalls in the middle and upper Yellow River basin in flood season and the corresponding atmosphere circulation pattern. The studied area could be divided into plateau area, arid area and monsoon area if the climate zone and the local river system were concerned. The heterogeneity of the three areas was evaluated with the strong precipitation concentration period (SCP) and the strong precipitation concentration degree (SCD). The results were summarized as follows: (1) The dependence of the precipitation on the strong rainfall was obvious in most area of the middle and upper Yellow River basin. The middle Shannxi Province and southern Shanxi province had fare intra-seasonal even distributed rainfalls, while Hetao area and northern Shaanxi province had some strong ones. (2) The average occurrence dates of the strong rainfall in flood season in plateau area was the earliest, followed by that in arid area, and then in monsoon area with a five-day delay. In south of the monsoon area, just Weihe, Jinghe and Luohe Basin and in east of the plateau area, the SCP changed greatly. In the 1990s, there took place significant decrease mutations of the SCP both in arid area and monsoon area, and that in arid area was earlier than that in monsoon area. (3) In the arid area, the high circulation situation in the SCP anomalous years showed that there would be strong rainfall in front of or behind of the flood season when the Western Pacific Subtropic High (WPSH) at 500 hPa on the northern side of 30°N, around 120°E, and the Southern Asia High (SAH) at 200 hPa on the eastern side of 120°E, around 30°N, moved towards each other or backwards each other. In the monsoon area, there was the same phenomenon as in the arid area when the WPSH located in 26°-30°N, around 120°E, meanwhile the SAH on the western side of 120°E, around 30°N.

Key words: middle and upper Yellow River, strong precipitation concentration period (SCP), strong precipitation concentration degree(SCD), intra-seasonal heterogeneity, atmosphere circulation

中图分类号:

P426.6

王楠, 李栋梁, 张杰. 黄河中上游季节内强降水的时间非均匀性特征及其对大气环流的响应[J]. 中国沙漠, 2013, 33(1): 239-248.

WANG Nan, LI Dong-liang, ZHANG Jie. The Intra-Seasonal Heterogeneity of the Strong Precipitation Events and the Corresponding Atmosphere Circulation Characteristics in the Middle and Upper Yellow River Basin in Flood Season[J]. JOURNAL OF DESERT RESEARCH, 2013, 33(1): 239-248.

参考文献

[1]Xu J.A study of anthropogenic seasonal rivers in China[J].CATENA,2004,55(1):17-32.

[2]Yang D W,Li C,Hu H P,et el.Analysis of water resources variability in the Yellow River of China during the last half century using historical data[J].Water Resources Research,2004,40,W06502.

[3]李林,汪青春,张国胜,等.黄河上游气候变化对地表水的影响[J].地理学报,2004,59(5):716-722.

[4]杨特群,饶素秋,陈冬伶.1951年以来黄河流域气温和降水变化特点分析[J].人民黄河,2009,31(10):76-77.

[5]邵晓梅,许月卿,严昌荣.黄河流域降水序列变化的小波分析[J].北京大学学报(自然科学版),2006,42(4):503-509.

[6]Fu G B,Chen S,Liu C M. Hydro-climatic trends of the Yellow River basin for the last 50 years[J].Climatic Change,2004,65:149-178.

[7]祝青林,张留柱,于贵瑞,等.近30年黄河流域降水量的时空演变特征[J].自然资源学报,2005,20(4):477-452.

[8]杨晓丹,翟盘茂.我国西北地区降水强度、频率和总量变化[J].科技导报,2005,23(6):24-26.

[9]杨金虎,江志红,王鹏祥,等.中国西北极端降水事件年内非均匀性特征分析[J].中国沙漠,2008,28(1):178-184.

[10]白虎志,李栋梁,陆登荣,等.西北地区东部夏季降水日数的变化趋势及其气候特征[J].干旱地区农业研究,2005,23(3):133-140.

[11]Zhang L J,Qian Y F. Annual distribution features of the yearly precipitation in China and their interannual variations[J].Acta Meteorologica Sinica,2003,17(2):146-163.

[12]魏娜,巩远发,孙娴,等.西北地区近50 a降水变化及水汽输送特征[J].中国沙漠,2010,30(6):1450-1457.

[13]蓝永超,马全杰,康尔泗,等.ENSO循环与黄河上游径流的丰枯[J].中国沙漠,2002,22(3):262-266.

[14]陈磊,王式功,尚可政,等.中国西北地区大范围极端高温事件的大气环流异常特征[J].中国沙漠,2011,31(4):1052-1058.

[15]陈权亮,刘晓冉,范广洲,等.川西高原夏季降水变化特征及其异常年环流形势[J].中国沙漠,2010,30(3):706-711.

[16]周顺武,张人禾.青藏高原地区上空NCEP/NCAR再分析温度和位势高度资料与观测资料的比较分析[J].气候与环境研究,14(2):284-292.

[17]Bonsal B R,Zhang X,Vincent L A,et al. Characteristics of daily and extreme temperatures over Canada[J].Journal of Climate,2001,14:1959-1976.

[18]陈冬冬,戴永久.近五十年我国西北地区降水强度变化特征[J].大气科学,2009,33(5):923-935.

[19]刘贤赵,李嘉竹,宿庆,等.基于集中度与集中期的径流年内分配研究[J].地理科学,2007:27(6):791-795.

[20]宋连春,张存杰.20世纪西北地区降水量变化特征[J].冰川冻土,2003,25(2):143-148.

[21]汤绪,钱维宏,梁萍.东亚夏季风边缘带的气候特征[J].高原气象,2006,25(3):375-381.

[22]江志红,何金海,李建平,等.东亚夏季风推进过程的气候特征及其年代际变化[J].地理学报,2006,61(7):675-686.

[23]王慧,李栋梁.卫星遥感结合地面观测资料对中国西北干旱区地表热力输送系数的估算[J].大气科学,2010,34(5):1026-1034.

[24]叶燕华,李栋梁,陈晓光.黄土高原春季降水对青藏高原感热异常的响应[J].中国沙漠,2007,27(2):315-319.

[25]汤绪,陈葆德,梁萍,等.有关东亚夏季风北边缘的定义及其特征[J].气象学报,2009,67(1):83-89.

[26]黄菲,李栋梁,汤绪,等.用过程透雨量确定的东亚夏季风北边缘特征[J].应用气象学报,2009,20(5):530-538.

[27]郭江勇,李耀辉.中国西北地区夏季降水的气候特征[J].干旱区研究,2006,23(3):489-494.

[28]贺皓,罗慧,黄宝霞.陕西盛夏多雨年与少雨年的大气环流特征分析[J].中国沙漠,2007,27(2):342-346.

[29]黄燕燕,钱永甫.长江流域、华北降水特征与南亚高压的关系分析[J].高原气象,2004,23(1):68-74.

[30]张琼,吴国雄.长江流域大范围旱涝与南亚高压的关系[J].气象学报,2001,59(5):569-577.