UBC Faculty Research and Publications

Boreal ecosystems sequestered more carbon in warmer years Higuchi, Kaz 2011

You don't seem to have a PDF reader installed, try download the pdf

Item Metadata


Black_AGU_2006GL025919.pdf [ 274.35kB ]
JSON: 1.0041924.json
JSON-LD: 1.0041924+ld.json
RDF/XML (Pretty): 1.0041924.xml
RDF/JSON: 1.0041924+rdf.json
Turtle: 1.0041924+rdf-turtle.txt
N-Triples: 1.0041924+rdf-ntriples.txt

Full Text

Boreal ecosystems sequestered more carbon in warmer years Jing M. Chen,1 Baozhang Chen,1 Kaz Higuchi,2 Jane Liu,3 Douglas Chan,2 Douglas Worthy,2 Pieter Tans,4 and Andy Black5 Received 5 February 2005; revised 20 March 2005; accepted 13 April 2005; published 19 May 2006. [1] A 13-year (1990–1996, 1999–2004), hourly air CO2 record measured on a 40 m tower in northern Canada is analyzed against interpolated marine boundary layer CO2 data representing the free troposphere above the tower. In warmer years, the planetary boundary layer was more depleted with CO2, suggesting that the land area (10 3– 104 km2) upwind of the tower sequestered more carbon. After using a novel approach to derive the photosynthetic flux from the air CO2 diurnal variation pattern, it is confirmed that boreal ecosystem photosynthesis increased more than ecosystem respiration in warmer years. Citation: Chen, J. M., B. Chen, K. Higuchi, J. Liu, D. Chan, D. Worthy, P. Tans, and A. Black (2006), Boreal ecosystems sequestered more carbon in warmer years, Geophys. Res. Lett., 33, L10803, doi:10.1029/2006GL025919. 1. Introduction [2] Atmospheric measurements, as interpreted using at- mospheric transport models [Tans et al., 1990; Denning et al., 1995; Gurney et al., 2002; Rodenbeck et al., 2003] and global carbon budgets based on land use history [Houghton et al., 1999] suggest the existence of a strong carbon sink on land, but the mechanisms are still uncertain [Pacala et al., 2001; Caspersen et al., 2001; Field and Fung, 1999]. At high latitudes, the impacts of temperature change on eco- systems are of great concern [Braswell et al., 1997; Oechel et al., 2000]. Greater biospheric activities at higher temper- atures were inferred from remote sensing [Myneni et al., 1997] and atmospheric CO2 measurements [Keeling et al., 1996]. From micrometeorological measurements at the stand level, some studies [e.g., Goulden et al., 1998] found that warming increased carbon release more than uptake in a boreal forest, while others [e.g., Black et al., 2000] showed the opposite. The effect of temperature on the forest carbon cycle is highly variable depending on species, age and stand history [Chen et al., 2003], and the boreal landscape consists of fragmented forest patches of various ages on variable soils and mixed with grassland and tundra due to frequent fire and insect disturbances as well as human activities. How these ecosystems collectively respond to climate change is, therefore, important in understanding the mechanisms controlling regional and global carbon cycles, as boreal forests globally store 13% of carbon in above- ground biomass and 43% in soil organic matter [Schlesinger, 1991; Jarvis et al., 2000]. CO2 fluxes mea- sured on micrometeorological towers in many flux networks worldwide [Baldocchi et al., 2001] have provided useful information on how various ecosystems behave under different climates. However, such towers can only sample a very small fraction of the land surface as each can only represent a footprint area of about 1 km2. We seek ways to retrieve carbon cycle information from atmospheric CO2 concentration measurements, which have much larger foot- prints (103–104 km2) [Lin et al., 2003] than flux towers. 2. Data and Site [3] A 13-year (1990–1996, 1999–2004), hourly aver- aged air CO2 concentration record measured on a 40-m tower at Fraserdale , nor thern Ontar io , Canada (4952029.900N, 8134012.300W), is used for this purpose (no data were collected from January 1997 to June 1998). The measurements were made according to the WMO (Global Atmospheric Watch) guidelines, with an accuracy of 0.1 ppm [Higuchi et al., 2003]. Temperature, humidity and wind speed at 20 m and 40 m and precipitation were also measured, allowing for accurate vertical mixing simu- lations under various atmospheric stability conditions. The interannual variation in air temperature was very similar to that at the weather station Kapuskasing, 87 km southwest of Fraserdale. The Globalview CO2 matrix data in 41 latitudi- nal bands based on weekly flask samples in the marine boundary layer (MBL) for the 13 years [Conway et al., 1994] were linearly interpolated to represent CO2 concen- tration in the free troposphere (FT) at the site as the top boundary condition of the planetary boundary layer (PBL). According to a Landsat TM image at a 30 m resolution acquired in 1998, the landscape (3600 km2 around the tower) consists of 66% of black spruce (Picea mariana) and Jack pine (Pinus banksiana), 20% open land after forest fires and logging, 11% aspen (Populus tremuloides) and paper birch (Betula papyrifera), and 3% open water. In the prevailing northwest wind direction, the forests are predom- inantly undisturbed. 3. Modeling Methodology [4] The diurnal variation in CO2 concentration above vegetation depends on the magnitudes of nighttime ecosys- tem respiration and daytime net photosynthesis. Atmospheric diffusion also contributes to the diurnal variation because the strength of vertical mixing varies greatly from nighttime to daytime. For the purpose of retrieving ecosystem infor- mation from atmospheric CO2 data, we used a model to simulate both ecosystem and atmospheric processes. The model consists of two components: (1) Boreal Ecosystem GEOPHYSICAL RESEARCH LETTERS, VOL. 33, L10803, doi:10.1029/2006GL025919, 2006 1Department of Geography, University of Toronto, Canada. 2Meteorological Service of Canada, Toronto, Canada. 3Department of Physics, University of Toronto, Toronto, Canada. 4CMDL/NOAA, Boulder, Colorado, USA. 5Department of Soil Science, University of British Columbia, Vancouver, Canada. Copyright 2006 by the American Geophysical Union. 0094-8276/06/2006GL025919$05.00 L10803 1 of 4 Productivity Simulator (BEPS) [Liu et al., 2002], which simulates ecosystem processes including water balance, photosynthesis [Farquhar et al., 1980], and autotrophic and heterotrophic respiration, and radiation and energy balances of the canopy and the soil surface; and (2) the Vertical Diffusion Scheme (VDS) [Chen et al., 2004], which simulates CO2 diffusion within the planetary boundary layer (PBL) under both stable and unstable atmospheric condi- tions. The combined BEPS-VDS model simulated well the measured hourly CO2 concentration at 40 m for the 13 years (r2 = 0.71, the root mean square error, RMSE = 5.32 ppm, n = 103858). For 10-day averaged hourly values, the agreement between measurements and the model is signif- icantly improved (r2 = 0.84, RMSE = 1.06 ppm, n = 11306) as the effects of horizontal advection and infrequent strong vertical diffusion associated with synoptic events become less significant in longer time periods. The 10-day averaged diurnal amplitudes of measured and modeled CO2 agree very well (r2 = 0.96) over the 13 years. [5] In order to gain information on ecosystem behavior, a methodology is developed to separate the effects of atmo- spheric diffusion and ecosystem metabolism on the CO2 concentration measurements. Figure 1 shows an example of measured and simulated hourly CO2 concentrations on a typical day (11 July 1996). The simulated values generally follow closely the measured values in the diurnal cycle. To investigate the effect of daytime photosynthesis on the measured CO2, we turned off the gross primary productivity (GPP) in BEPS from sunrise to sunset. As shown in Figure 1, the simulated CO2 with GPP = 0 increases considerably from the measured CO2. This increase is expected as the carbon uptake by photosynthesis is artifi- cially terminated while the total ecosystem respiration (both heterotrophic and autotrophic) remains unchanged. As at- mospheric diffusion is unchanged in both simulations and has the same effect on the measured and modeled CO2, the difference between the simulated and measured values is therefore solely due to photosynthesis. In this way, the signal of photosynthesis is extracted from the CO2 time series. Physically, the hourly average difference in CO2 (DCi, in ppm) between the measured and simulated (with GPP = 0) cases reflects the accumulating reduction of CO2 by GPP. Assuming that this reduction is uniform in the mixed layer, the simulated mixed layer height (zi) and the average dry air density (rair) can then be used to estimate the time-integrated (since sunrise) GPP per unit surface area as DCirairzi (mol m 2). As the air moves across the landscape, this effect of GPP on air CO2 gradually accu- mulates. For hour i after sunrise, the total accumulated effect is DCirairzi, and GPP in this hour is (DCi rair zi  DCi1 rairzi1, in mol m 2). The daily total GPP then equals PSS i¼SRþ1 DCizi  DCi1zi1ð Þ rair, where SR is the hour of sunrise and SS is sunset. The accumulation of this photosynthesis effect starts at sunrise and moves with the air from sunrise to sunset, and the tower CO2 measurements therefore integrate the influence of the land surface of daily air travel length upwind of the tower. This simple method- ology makes no assumptions related to horizontal homoge- neity. Since no flux measurements were made at the Fraserdale site, this methodology was validated at a tower flux site in a black spruce forest in Saskatchewan, where the upwind area is covered by forests of similar density. Half hourly carbon fluxes in 1999 were converted into GPP using an existing method developed at the Saskatchewan site [Griffis et al., 2003], and the concentration-derived daily GPP was highly correlated with that derived from eddy covariance flux measurements (r2 = 0.82, RMSE = 0.11 g C m2 d1, n = 186). 4. Results and Discussion [6] A simple analysis of the CO2 record against FT data reveals important temperature- dependent ecosystem signals (Figure 2a): the annual mean difference in CO2 (DCFT-PBL) between FT and the daily minimum measured at 40 m increased with the annual mean air temperature. The daily minimum CO2 value represented closely the mean value in the well mixed PBL [Chen et al., 2004, 2005], and the daily DCFT-PBL resulted from the net difference between gross primary productivity (GPP) in daytime and ecosystem respiration (ER) in both nighttime and daytime, as well as the mixing between FT and PBL [Bakwin et al., 1998]. The increase in the annual mean DCFT-PBL with temperature suggests that GPP increased considerably faster with tem- perature than did ER. Daily balloon temperature soundings at Moosonee (200 km N from Faserdale) and Maniwaki (540 km SE) weather stations in the same years were used to determine the very weak correlations between the annual PBL height and the annual mean temperature (r2 = 0.12 and 0.19, respectively). The PBL height increased 2% and 5% from the coldest to warmest year at these two locations, respectively, and bias estimates in Figure 2a are based on the 5% increase. The difference in the frequency of south- erly or northerly airflows was about 4% between two coldest (1992 and 1993) and two warmest (1999 and 2001) years. Since southerly flows had a lower CO2 concentration than the northerly flows by 1 ppm in the growing season (largest in the year), the flow direction had Figure 1. An example of modeled and measured hourly values of atmospheric CO2 on 11 July 1996 at 40 m at Fraserdale. The agreement indicates that both ecosystem metabolism (photosynthesis and respiration) and atmo- spheric diffusion are well modeled. A new series is obtained from sunrise to sunset (indicated by triangles) after turning off the gross primary productivity (GPP) in the model. In the absence of GPP, the concentration remained higher than the corresponding measured values. The vertical line is the difference between measured and simulated (with GPP = 0) CO2, that is, DCi used for estimating the cumulative difference resulting from GPP since sunrise. L10803 CHEN ET AL.: BOREAL ECOSYSTEMS L10803 2 of 4 small impacts on DCFT-PBL on a yearly basis depending on the frequency. The total bias error from these two largest sources would only decrease, to the largest extent possible, the slope of DCFT-PBL against temperature (Figure 2a) by 15%. The annual mean air pressure and temperature were uncorrelated at Fraserdale for the 13 years and Kapuskasing for 20 years (r2 = 0.14 and 0.0003, respectively), suggesting that the frequency of low and high pressure systems affecting the vertical mixing regime had only very small interannual variations. The coldest year of 1992 after the Pinatubo volcano eruption is an outlier possibly because of the positive effect of the increased diffuse radiation on photosynthesis. Without the 1992 data point, the r2 value increases to 0.87. [7] Seasonal variations in DCFT-PBL (Figure 2b) reveal the reason for its large temperature sensitivity. In winters, marked by daily mean temperature (T) below 5C, DCFT-PBL was negative and decreased slowly with increas- ing T, indicating a small increase of ER with temperature. At T > 0, DCFT-PBL increased rapidly, suggesting that the net uptake of CO2 by the surface, that is GPP-ER, increased rapidly with T. As the T increase in the growing season (May-August) was only slightly less than the annual T increase (65–85%), an increase in the annual T resulted in an increase in the net carbon uptake. The actual amount of the net carbon uptake (in mol C m2 t1, where t is a time period of interest) equals the change in DCFT-PBL (in ppm t1 or 44.64  106 mol C m3 t1 at the sea level and T = 273K) times the mixed layer height (m). Since the mixed layer height in summers was about 50% higher than that in winters, we expect that the difference in the temperature sensitivity of (GPP – ER) between summers and winters was also about 50% larger than what is indicated as the slope in Figure 2b. This also confirms the importance of the timing of spring warming in ecosystem carbon cycling. [8] Using the methodology described in Section 2, daily GPP values are derived and summed to annual values. A strong linear relationship is found between the annual concentration-derived GPP and annual mean air temperature (r2 = 0.71, or 0.69 for active growing season mean temper- ature) (Figure 3). Other meteorological factors were weakly correlated with GPP (r2 = 0.04 and 0.13 for precipitation and radiation, respectively). The ratio of annual evapotrans- piration modeled by BEPS to precipitation ranged from 0.40 to 0.73 in these 13 years, suggesting that water was not a limiting factor for growth in this area. Also shown in Figure 3 is the annual ER modeled with consideration of both temperature and moisture effects [Lloyd and Taylor, 1994; Potter, 1997] using a multiple layer soil model. The actual modeled ER has an equivalent Q10 value of 2.4 because of the increase in the active layer in summers. The ER modeling is constrained (to <4%) by the CO2 concen- tration measurements, as the nighttime CO2 increase to the maximum was highly sensitive to ER, especially in calm nights with a large T inversion, when a 4% increase in ER caused a 1.0 ppm increase in modeled CO2 concentration at 40 m. An optimization method was used to find ER model parameters that produce the minimum RMSE between modeled and measured CO2 at 40 m. Consistent with the finding that the net uptake of CO2 by ecosystems increased with T (Figure 2), the concentration-derived GPP had a larger T sensitivity than that of ER (Figure 3). Figure 2. Interannual and seasonal temperature dependen- cies of atmospheric CO2 over a boreal region. (a) The annually-averaged difference in CO2 (DCFT-PBL) between the daily minimum in the planetary boundary layer (PBL) and the free troposphere (FT) increased with air tempera- ture. The vertical bars indicate bias errors due to temperature dependencies of the mixed layer height (left of each data point) and the wind direction (right of each data point). This increase in DCFT-PBL suggests that the PBL is more depleted with CO2 in warmer years. The slope of DCFT-PBL against temperature is highly significant (p < 0.0008 in the t test). (b) 10-day mean DCFT-PBL values vs. temperature (T), indicating that in the growing season (T > 0C) an increase in air temperature generally induced an increase in the PBL CO2 depletion. Figure 3. Sensitivities of gross primary productivity (GPP) and ecosystem respiration (ER) to temperature in boreal ecosystems. The vertical bars indicate their errors. The concentration-derived GPP increased more with temperature than did ER, providing a reason for the larger PBL CO2 depletion in warmer years (Figure 2). The standard error in the slope against temperature is 0.1184 and 0.1091 mol m2y1C1 for GPP and ER, respectively, and these two slopes are significantly different in the t test (p < 0.017). L10803 CHEN ET AL.: BOREAL ECOSYSTEMS L10803 3 of 4 [9] We used the same model to explore the possible reasons for the difference in the T sensitivity between GPP and ER. The large T sensitivity of GPP shown in Figure 3 could not be captured by the model (r2 = 0.54, RMSE = 20.5 g C m2y1) when the nutrient availability was kept constant, but was well simulated (r2 = 0.79, RMSE = 8.3 g C m2y1) when coupled carbon (C) and nitrogen (N) dynamics in soil and vegetation were included [Chen et al., 2003] based on C:N ratios of vegetation and soil [Dickinson et al., 2002]. At higher T, the decomposition of soil organic matter is faster, producing more mineralized N available for immediate uptake by plant roots [Braswell et al., 1997; Jarvis et al., 2000]. As boreal ecosystems are nutrient limited and plant growth is sensitive to the amount of available nitrogen, more mineralized N at higher T leads to higher productivity. These model experiments, though explorative, suggest that nutrient conditions in the soil played an important role in the response of boreal ecosys- tems to T changes [Jarvis et al., 2000], in agreement with N mineralization data from a 10-year soil heating experiment in a temperate forest [Melillo et al., 2002]. Our result is in general agreement with the finding from a 5-year, 5C soil warming experiment inducing an accumulated increase of about 80% in growth in a boreal forest [Jarvis et al., 2000]. This suggests that in global carbon cycle modeling, it is important to consider coupled carbon and nutrient dynamics. [10] The retrieved GPP and ER values constrained by the concentration measurements suggest that boreal ecosystems in the vicinity of the Fraserdale tower were collectively a carbon sink of 10.8 ± 14.2 g C m2 y1 in these 13 years, which is in agreement with previous work based on remote sensing [Chen et al., 2003]. However, the uncertainties in the absolute values of GPP and ER are still of the same order of magnitude as the difference between them. As the record gets longer, these uncertainties would become smaller. Tower flux measurements allow immediate assess- ments of carbon balance within a small footprint, while concentration measurements can provide reliable informa- tion on the ecosystem response to climate change for much larger areas. The fact that the temperature sensitivity of GPP is larger than that of ER suggests that global warming could lead to increased carbon sequestration in boreal ecosystems. [11] Acknowledgments. This work is supported by the Canadian Foundation for Climate and Atmospheric Sciences. Lin Huang and Alexander Shashkov of Atmospheric Science and Technology Directorate, Environment Canada provided useful comments. References Bakwin, P. S., et al. (1998), Measurements of carbon dioxide on very tall towers: Results of the NOAA/CMDL program, Tellus, Ser. B, 50, 401– 415. Baldocchi, D., et al. (2001), Fluxnet: A new tool to study the temporal and spatial variability of ecosystem-scale carbon dioxide, water vapour, and energy flux densities, Bull. Am. Meteorol. Soc., 82, 2415–2434. Black, T. A., W. J. Chen, A. G. Barr, M. A. Arain, Z. Chen, Z. Nesic, E. H. Hogg, H. H. Neumann, and P. C. Yang (2000), Increased carbon seques- tration by a boreal deciduous forest in years with a warm spring, Geo- phys. Res. Lett., 27, 1271–1274. Braswell, B. H., D. S. Schimel, E. Linder, and B. Moore (1997), The response of global terrestrial ecosystems to interannual temperature varia- bility, Science, 278, 870–872. Caspersen, J. P., et al. (2001), Contributions of land-use history to carbon accumulation in U.S. forests, Science, 290, 1148–1151. Chen, J. M., et al. (2003), Spatial distribution of carbon sources and sinks in Canada’s forests, Tellus, Ser. B, 55, 622–641. Chen, B., J. M. Chen, J. Liu, D. Chan, K. Higuchi, and A. Shashkov (2004), A vertical diffusion scheme to estimate the atmospheric rectifier effect, J. Geophys. Res., 109, D04306, doi:10.1029/2003JD003925. Chen, B., J. M. Chen, and D. E. J. Worthy (2005), Interannual variability in the atmospheric CO2 rectification over a boreal forest region, J. Geophys. Res., 110, D16301, doi:10.1029/2004JD005546. Conway, T. J., P. P. Tans, L. S. Waterman, K. K. Thoning, D. R. Kitzis, K. A. Masarie, and N. Zhang (1994), Evidence for interannual variability of the carbon cycle from the National Oceanic and Atmospheric Admin- istration/Climate Monitoring and Diagnostics Laboratory Global Air Sampling Network, J. Geophys. Res., 99(D11), 22,831–22,856, (Data available at www.cmdl.noaa.gov/ccgg/) Denning, A. S., I. Y. Fung, and D. A. Randall (1995), Latitudinal gradient of atmospheric CO2 due to seasonal exchange with land biota, Nature, 376, 240–243. Dickinson, R. E., et al. (2002), Nitrogen controls on climate model evapo- transpiration, J. Clim., 15, 278–295. Farquhar, G. D., S. Caemmerer, and S. Berry (1980), A biochemical model of photosynthetic CO2 assimilation in leaves of C3 species, Planta, 149, 78–90. Field, C. B., and I. Y. Fung (1999), The not-so-big U.S. carbon sink, Science, 285, 544–545. Goulden, M. L., et al. (1998), Sensitivity of boreal forest carbon balance to soil thaw, Science, 279, 214–217. Griffis, T. J., et al. (2003), Ecophysiological controls on the carbon balances of three southern boreal forests, Agric. For. Meteorol., 117, 53–71. Gurney, R. K., et al. (2002), Towards robust regional estimates of CO2 sources and sinks using atmospheric transport models, Nature, 415, 626–630. Higuchi, K., et al. (2003), Regional source/sink impact on the diurnal, seasonal and inter-annual variations in atmospheric CO2 at a boreal forest site in Canada, Tellus, Ser. B, 55, 115–125. Houghton, R. A., J. L. Hachler, and K. T. Lawrence (1999), The U.S. carbon budget: Contributions from land-use change, Science, 285, 574–578. Jarvis, P., E. Linder, and S. Botany (2000), Constraints to growth of boreal forests, Nature, 405, 904–905. Keeling, R. F., S. C. Piper, and M. Heimann (1996), Global and hemi- spheric CO2 sinks deduced from changes in atmospheric O2 concentra- tion, Nature, 381, 218–221. Lin, C., et al. (2003), A near-field tool for simulating the upstream influence of atmospheric observations: The stochastic time-inverted lagrangian transport (STILT) model, J. Geophys. Res., 108(D16), 4493, doi:10.1029/2002JD003161. Liu, J., et al. (2002), Net primary productivity mapped for Canada at 1–km resolution, Global Ecol. Biogeogr., 11, 115–129. Lloyd, J., and J. A. Taylor (1994), On the temperature dependence of soil respiration, Fuct. Ecol., 8, 315–323. Melillo, J. M., et al. (2002), Soil warming and carbon-cycle feedbacks to the climate system, Science, 298, 2173–2176. Myneni, R. B., et al. (1997), Increased plant growth in the northern high latitudes from 1988 to 1991, Nature, 386, 698–702. Oechel, W. C., et al. (2000), Acclimation of ecosystem CO2 exchange in the Alaskan Arctic in response to decadal climate warming, Nature, 406, 978–981. Pacala, S. W., et al. (2001), Consistent land- and atmospheric-based US carbon sink estimates, Science, 292, 2316–2320. Potter, C. S. (1997), An ecosystem simulation model for methane produc- tion and emission from wetlands, Global Biogeochem. Cycles, 11, 495– 506. Rodenbeck, C., et al. (2003), CO2 flux history 1982–2001 inferred from atmospheric data using a global inversion of atmospheric transport, Atmos. Chem. Phys., 3, 1919–1964. Schlesinger, W. H. (1991), Biogeochemistry: An Analysis of Global Change, Elsevier, New York. Tans, P. P., I. Y. Fung, and T. Takahashi (1990), Observation constraints on the global atmospheric CO2 budget, Science, 247, 1431–1438.  A. Black, Department of Soil Science, University of British Columbia, MCML 129 - 2357 Main Mall, Vancouver, BC, Canada V6T 1Z4. D. Chan, K. Higuchi, and D. Worthy, Meteorological Service of Canada, 4905 Dufferin Street Downsview, Toronto, ON, Canada M3H 5T4. B. Chen and J. M. Chen, Department of Geography, University of Toronto, 100 St. George St., Room 5047, Toronto, ON, Canada M5S 3G3. (chenj@geog.utoronto.ca) J. Liu, Department of Physics, University of Toronto, 60 St. George St., Toronto, ON, Canada M5S 1A7. P. Tans, CMDL/NOAA, 325 Broadway R/GMD1, Boulder, CO 80305– 3328, USA. L10803 CHEN ET AL.: BOREAL ECOSYSTEMS L10803 4 of 4


Citation Scheme:


Usage Statistics

Country Views Downloads
Japan 3 0
Canada 2 0
China 2 1
City Views Downloads
Tokyo 3 0
Vancouver 2 0
Beijing 2 0

{[{ mDataHeader[type] }]} {[{ month[type] }]} {[{ tData[type] }]}


Share to:


Related Items