地理科学进展 ›› 2014, Vol. 33 ›› Issue (8): 1029-1038.doi: 10.11820/dlkxjz.2014.08.003
出版日期:
2014-08-25
发布日期:
2014-08-25
作者简介:
作者简介:杨旺明(1989-),男,甘肃天水人,硕士研究生,研究方向为城市化与区域气候,E-mail:
基金资助:
Wangmin YANG(), Chong JIANG, Xiaoyong YU, Xuefeng CUI(
)
Online:
2014-08-25
Published:
2014-08-25
摘要:
人为热是指由人类活动产生而释放到大气中的热量,这部分热量以感热和潜热的形式释放到城市冠层和城市边界层中,是城市生态系统的重要能量来源之一。在城市系统中,建筑物、交通运输和人类新陈代谢所释放的热量构成了总的人为热,具有明显的日变化和季节变化特征:清晨和傍晚出现一天中的两大峰值,而冬季和夏季分别是全年中最显著的两个季节。人为热的计算方法通常分为仪器观测法和能源消费清单法,其中能源消费清单法是目前普遍使用的方法。人为热主要通过改变大气的热力学能量方程和水汽方程中的热量和水汽量来影响区域和全球气候。在城市中,人为热是冬季和夜间城市热岛形成的主要原因,会影响大气边界层的稳定度和增加边界层高度。在全球范围内,人为热会对大气环流产生扰动,但对全球增温效应不显著。随着全球能源消费和人口的增加,人为热将成为气候变化的重要人为因子之一,因此如何观测和估算出一套高精度的人为热数据集极为重要。
中图分类号:
杨旺明, 蒋冲, 喻小勇, 崔雪锋. 气候变化背景下人为热估算和效应研究[J]. 地理科学进展, 2014, 33(8): 1029-1038.
Wangmin YANG, Chong JIANG, Xiaoyong YU, Xuefeng CUI. Review of research on anthropogenic heat under climate change[J]. PROGRESS IN GEOGRAPHY, 2014, 33(8): 1029-1038.
表1
人为热的气候效应"
研究区域 | 气候模式 | 城市冠 层模式 | 温度 | 降水 | 边界层 稳定度 | 边界层 高度 | 文献 |
---|---|---|---|---|---|---|---|
费城 | MM5 | +,冬天城市热岛增温幅度为2~3℃ | + | Fan et al, 2005 | |||
东京 | CSU-MM | +,温度的峰值出现在早上8:00, 与其对应的人为热最大 | Ichinose et al, 1999 | ||||
东京 | MM, CM BEM (多模式集成) | CM | +, 温度对电力消费的敏感度为6.6%/℃,人为热释放的高度对增温幅度影响较小 | Kondo et al, 2003 | |||
斯洛坎区 埃德蒙顿, 多伦多, 纽约 蒙特利尔 | GEM | +, 晚上平均增温幅度,温哥华为2℃,芝 加哥2℃,底特律1.5℃,多伦多 2.5℃,蒙 特利尔2℃,纽约超过4.5℃,洛杉矶超过5.1℃ | + | + | Makar et al, 2006 | ||
杭州 | NJU-RBLM | +,人为热对城市热岛效应的贡献冬天 为54.5%,夏天为43.6% | + | Chen et al, 2008 | |||
京阪神 | WRF | UCM | +,夜晚的增温幅度是白天的3倍 | Narumi et al, 2009 | |||
西欧 | REMO | +,平均增温幅度在0.15~0.5℃之间,地 形影响没有排除 | 不显著 | Block, 2004 | |||
中国 | WRF | UCM | +,在长三角地区的增温幅度为2℃,人 为热的贡献为0.6℃ | 京津塘地区降水量增加6.65%,长江三角洲地区降低2.54% | + | + | Feng et al,2012 |
全球 | CAM | +,在热带地区温度会增加1~2℃,而北 美和亚洲地区会增加8℃ | Washington, 1972 | ||||
全球 | UKMO | +,变化不明显,但是人为热有明显的区 域敏感性 | 印度尼西亚增加19 mm/d,热带大西洋增加32 mm/d,影响最大地区为热带 | Murphy et al, 1976 | |||
全球 | CAM | +, 全球平均增温为0.15℃,到2010年会 增温0.4~0.9℃ | + | + | Flanner, 2009 | ||
全球 | CAM | +,全球增温不显著,全球平均增温为0.01℃,季节平均为0.02℃,冬天高纬度 地区增温为1℃,对大气环流起扰动作用 | Zhang et al, 2013 |
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