从第三极到北极： 热喀斯特及其对碳循环影响研究进展
贾麟1(
), 范成彦1, 母梅1, 陈旭1, 仲文1, 尚建国2, 张凤1, 李丽丽3, 彭小清1, 牟翠翠1,4,5(), 张廷军1,5
), 范成彦1, 母梅1, 陈旭1, 仲文1, 尚建国2, 张凤1, 李丽丽3, 彭小清1, 牟翠翠1,4,5(), 张廷军1,5
Studies of thermokarst and its effects on ecosystem carbon cycle in the Third Polar regions and the Arctic
Lin JIA1(), Chengyan FAN1, Mei MU1, Xu CHEN1, Wen ZHONG1, Jianguo SHANG2, Feng ZHANG1, Lili LI3, Xiaoqing PENG1, Cuicui MU1,4,5(), Tingjun ZHANG1,5
), Chengyan FAN1, Mei MU1, Xu CHEN1, Wen ZHONG1, Jianguo SHANG2, Feng ZHANG1, Lili LI3, Xiaoqing PENG1, Cuicui MU1,4,5(), Tingjun ZHANG1,5
图3. 1997—2015年青藏高原祁连山区俄博岭地区热融滑塌发育过程（以2009年卫星影像作为基准影像）。1997—2009年和2009—2015年滑塌最宽处分别增加了24 m和30 m， 源头分别后退了23 m和29 m
Fig.3. The development of thaw slump on the Eboling mountains of the Qilian Mountains on the northern Qinghai-Tibet Plateau from 1997 to 2015 （based on 2009 satellite imagery）. The widest part of the slump widened by 24 m from 1997 to 2009， and widened by 30 m from 2009 to 2015； the source of the slump retreated 23 m from 1997 to 2009， and from 2009 to 2015 going back 29 m
