Wang M, Chen H, Wu N, Peng C, Zhu Q, Zhu D, Yang G, Wu J, He Y, Gao Y,
Tian J,Zhao X
QuaternaryScience Reviews, 2014, 99: 34-41.
Abstract:Understandingthe responses of the carbon-rich peatland ecosystems to past climate change iscrucial for predicting peat carbon fate in the future. Here we presented a datasynthesis of peatland initiation ages, area changes, and peat carbon (C)accumulation rate variations in China since the Holocene, along with total Cpool estimates. The data showed different controls of peatland expansion and Caccumulation in different regions. The peat C accumulation rates were 32.3(ranging from 20.7 to 50.2) g C m-2yr-1in theQinghai-Tibetan Plateau (QTP) and 14.7 (ranging from 7.4 to 36.5) g C m-2yr-1in the Northeast China (NEC). The peaks of peatland expansion and Caccumulation in the QTP occurred in the early Holocene in response to highsummer insolation and strong summer-winter climate seasonality. The rapidpeatland expansion and maximum C accumulation rate in the NEC occurred in themiddle-late Holocene. Peatlands scattered in the coastal and lakeside regionsof China expanded rapidly at the onset of the Holocene due to large transgression,consistent with the stronger summer insolation and monsoon, and during themiddle and late Holocene, as a response to the high and stable sea level andthe strong summer monsoon. The carbon storage of peatlands in China wasestimated as 2.17 (ranging from 1.16 to 3.18) Pg, among which 1.49 (rangingfrom 0.58 to 2.40) Pg was contributed by peatlands in the QTP, 0.21 (rangingfrom 0.11 to 0.31) Pg by those in the NEC, and 0.47Pg by those scattered inother regions of China. Our comparison of peatlands dynamics among regions inChina showed that climate and monsoon are the essential factors in determiningthe expansion and carbon accumulation patterns of peatlands, although theireffects on peatland formation and C accumulation is complex owing to landavailability in peatland basins and regional moisture conditions.