Methane emissions reduce the radiative cooling effect of a subtropical estuarine mangrove wetland by half

Abstract

The role of coastal mangrove wetlands in sequestering atmospheric carbon dioxide (CO ) and mitigating climate change has received increasing attention in recent years. While recent studies have shown that methane (CH ) emissions can potentially offset the carbon burial rates in low-salinity coastal wetlands, there is hitherto a paucity of direct and year-round measurements of ecosystem-scale CH flux (F ) from mangrove ecosystems. In this study, we examined the temporal variations and biophysical drivers of ecosystem-scale F in a subtropical estuarine mangrove wetland based on 3 years of eddy covariance measurements. Our results showed that daily mangrove F reached a peak of over 0.1 g CH -C m day during the summertime owing to a combination of high temperature and low salinity, while the wintertime F was negligible. In this mangrove, the mean annual CH emission was 11.7 ± 0.4 g CH -C m year while the annual net ecosystem CO exchange ranged between −891 and −690 g CO -C m year , indicating a net cooling effect on climate over decadal to centurial timescales. Meanwhile, we showed that mangrove F could offset the negative radiative forcing caused by CO uptake by 52% and 24% over a time horizon of 20 and 100 years, respectively, based on the corresponding sustained-flux global warming potentials. Moreover, we found that 87% and 69% of the total variance of daily F could be explained by the random forest machine learning algorithm and traditional linear regression model, respectively, with soil temperature and salinity being the most dominant controls. This study was the first of its kind to characterize ecosystem-scale F in a mangrove wetland with long-term eddy covariance measurements. Our findings implied that future environmental changes such as climate warming and increasing river discharge might increase CH emissions and hence reduce the net radiative cooling effect of estuarine mangrove forests. 2 4 4 CH4 CH4 CH4 4 CH4 4 4 2 2 CH4 2 CH4 CH4 4 −2 −1 –2 −1 −2 −1