Wildfire, soil and vegetation: new directions

Summary of papers

Fire frequency/area and climate change

(Williams 2016) find that a positive trend in PET accounts for  78 % of the positive trend in burned area since 1984 in W USA. The strength of the observed interannual relationship between PET and forest-fire area and the co-occurring positive trends suggest that (1) continued warming will promote continued increases in western USA forest-fire area while fuels are not limiting, consistent with previous empirical evaluations, and (2) other processes besides increased PET have also contributed to the increase in the western US forest fire area and will continue to do so.

Climate change will likely increase fire severity and occurrence across the boreal biome (Flannigan 1998) and with these changes, there will be an increase in total annual C emissions (Turetsky 2011).

Methods estimating C, N, biomass, soil losses

(Boby 2010) nicely estimates N and C emission in Alaska. They show have this can be done using mainly the adventitious-root-height method (ARH). The ARH method may, however, be ineffective for estimating pools in intense fires that leave trees uprooted, or in sites where trees were rooted within a layer of organic soil that was completely combusted, leaving no evidence of the rooting position of the prefire trees. They investigated 28 independent unburned stands and found that the average height of the highest adventitious roots on the stem corresponded to the surface of the moss layer; roots were, on average, 3.2 ± 0.43 cm below the surface of the green moss. This pattern was consistent across a range of understory moss communities, including feather mosses, Sphagnum spp., and other moss species

(Morgan 2014) We suggest that instead of collapsing many diverse, complex and interacting fire effects into a single severity index, the effects of fire should be directly measured and then integrated into severity index keys specifically designed for objective severity assessment. Using soil burn severity measures as examples, we highlight best practices for selecting imagery, designing an index, determining timing and deciding what to measure, emphasising continuous variables measureable in the field and from remote sensing.

(Pastick 2014) estimated soil organic layer thickness in Yukon.


(Amiro 2000) looks at NPP during the first 15 years. Most of the area have a NPP of carbon (C) around 150-300 g m-2 yr-1.Only the 1-3 since fire have no area with very high NPP (>350). All regions (more or less) show a positive correlation between NPP and time since fire. For each year NPP increases with roughly 10 g m-2 yr-1. One study area (Alberta boreal plains) has data up to 60 years after fire. Here, NPP increases up to  30 yr since fire and then slowly increases a bit more until 50-60 yrs since fire.

(Bond-Lamberty 2004)Total NPP was low (50–100 g C m-2 yr-1) immediately after fire, highest 12–20 years after fire (332 and 521gCm-2 yr-1 in the dry and wet stands, respectively) but 50 percent lower than this in the oldest stands. Tree NPP was highest 37 years after fire but 16–39 percent lower in older stands, and was dominated by deciduous seedlings in the young stands and by black spruce trees (85 percent) in the older stands. Bryophytes comprised a large percentage of aboveground NPP in the poorly drained stands, while belowground NPP was 0–40 percent of total NPP. Net ecosystem production (NEP), calculated using heterotrophic soil and woody debris respiration data from previous studies in this chronosequence, implied that the youngest stands were moderate C sources (roughly, 100 g C m-2 yr-1), the middle-aged stands relatively strong sinks (100–300g C m-2 yr-1), and the oldest stands about neutral with respect to the atmosphere. Source to sink occurred around 20-30 yrs after fire, both in wet and dry stands. Respiration of woody debri important up to 20-30 yrs after fire, at later stages its a very small C source.

(Mkhabela 2009) This study has shown that the fire sites had generally higher GEP, Re and ET than the harvested sites, which we believe is largely a result of greater species diversity at the fire sites coupled with higher soil water content. Regardless of disturbance history, NEP was generally negative for the younger sites, indicating that recently disturbed sites are C sources. C dynamics following fire may go through four phases compared to three phases for harvested sites: soon after fire, burned sites become C sources; then become C sinks; then become C sources again when the dead woody material starts decaying; and thereafter become C sinks or neutral. In contrast, harvested sites are C sources soon after harvest; C sinks at intermediate age; and then C neutral or a small sink at maturity. This hypothesised pattern is still very uncertain though.

Moss δ13C provides information about photosynthetic performance and relative growth rates, integrates moss photosynthetic activity throughout a growth period, and typically increases as a function of water availability (Rice 1996, Rice 2000). (Deane-Coe 2015) found that air warming also resulted in a consistent reduction in δ13C in all three mosses, and we found that δ13C was positively correlated with NPP in both years, as has been observed in other moss communities (Rice 2000). In contrast to vascular plants, where low δ13C values typically result from greater growth rates due to high water use efficiency, low δ13C values in mosses are most commonly observed when growth rates are low due to low tissue water content, when chloroplastic demand and diffusional resistance of CO2 are both low ((Rice 1996, Rice 2000). Collectively, the reduction in NPP and δ13C in two of the three dominant mosses at our site points to the possibility of drier conditions that reduced moss growth as a result of air warming.

(Alexander 2015) Global change models predict that high-latitude boreal forests will become increasingly susceptible to fire activity as climate warms, possibly causing a positive feedback to warming through fire-driven emissions of CO2 into the atmosphere. However, fire-climate feedbacks depend on forest regrowth and carbon (C) accumulation over the post-fire successional interval, which is influenced by nitrogen (N) availability. To improve our understanding of post-fire C and N accumulation patterns in boreal forests, we evaluated above- and belowground C and N pools within 70 stands throughout interior Alaska. Increased fire activity is also expected to volatilize nitrogen (N) (Harden and others 2002; Neff and others 2005; Boby and others 2010) in this already N-limited ecosystem (Van Cleve and Alexander 1981) because most N is stored in organic soils which are often greater than 50% consumed by fire (Kasischke and others 1995). Reduced N availability may limit forest productivity and regeneration and thus, C accumulation and storage during the post-fire interval (Harden and others 2000). Changes in the fire regime may also alter patterns of C and N accumulation by triggering patterns of forest regrowth that differ from the pre-fire stand. For example, increased fire frequency and extent can reduce seed availability (Romme and others 1998; Johnstone and Chapin 2006b), while increased fire severity can increase seed germination (Johnstone and Chapin 2006a). These changes in initial establishment parameters, combined with species-specific growth habits and competitive abilities, can alter stand composition and structure, and ultimately the rate and amount of C and N stored during post-fire succession (Weber and Flannigan 1997). Thus, the balance between fire-driven losses of C and N and their re-accumulation rates will determine whether increased fire activity creates a positive, neutral, or negative feedback to the climate system.

(Bona 2016)Tree canopy is intimately linked to site moisture, in part because of shading but also because black spruce trees are more productive (with less open canopies) when the water table is lower and a larger oxic rooting zone is provided. Therefore, our relationships between canopy and moss NPP are likely explained by soil moisture content differences between open and closed canopy systems. Water table depth, air humidity, or soil moisture information could improve prediction of moss NPP. However, since indicators of soil moisture or water table depth at a national scale a re lacking, this study suggests that tree canopy can be an effective proxy because canopy openness controls, as well as responds to, several light and moisture related variables. Results used in model. Although MOSS-C does not explicitly represent the paludification process, our results indicate the MOSS-C sub model’s potential ability to predict which sites are more likely to accumulate larger peat stocks over longer time frames, where high water tables can restrict tree roots and lower tree productivity, and to distinguish these from sites that tend to be dryer with more productive trees and smaller moss derived C pools. No significant relationships were found that could help describe potential sources of the unexplained finer scale variation in organic horizon C for these plots, suggesting that, to further improve the model, more detailed plot level data would be required. Also has fire in their model....

(Turetsky 2010) In Alaskan forests, moss abundance showed a unimodal distribution with time since fire, peaking 30–70 years post-fire. Mosses contributed 48% and 20% of wetland and upland productivity, respectively, but produced tissue that decomposed more slowly than both nonwoody and woody vascular tissues. The roles of moss traits in regulating key aspects of boreal performance (ecosystem N supply, C sequestration, permafrost stability, and fire severity) represent critical areas for understanding the resilience of Alaska’s boreal forest region under changing climate and disturbance regimes. REALLy good intro for highlightning mosses role. Eg. Mosses, one of the major groups of bryophytes, are ubiquitous and dominant components of ground-layer vegetation in both upland forests and peatlands across the boreal biome. These plants have received attention in several recent reviews for their importance in regulating soil hydroclimate and nutrient cycling in boreal ecosystems (van Breemen 1995; Turetsky 2003; Nilsson and Wardle 2005). Recent studies affiliated with the Bonanza Creek Long Term Ecological Research (BNZ-LTER) program also have documented relationships between moss composition and ecosystem parameters such as aboveground tree productivity and soil C storage (Hollingsworth et al. 2008) and have suggested that moss abundance plays a critical role in post-fire successional trajectories (Johnstone et al. 2010)


(Mkhabela 2009) Higher ET at the burned sites compared to harvested. The higher ET at the fire sites compared to the harvested sites was likely, in part, a result of the presence of both deciduous and coniferous trees. In addition, the fire sites had higher soil water content than the harvested sites, which might have enhanced ET.

(Kuglerová 2014) describes a hydrological model for boreal landscape using a high res DEM.

(Kuglerová 2015) Mapped groundwater discharge and found that it provided riparian-like habitat further away from the streams and also in upland-forest sites compared to the non-discharge counterparts. In addition, soil chemistry (C:N ratio, pH) and light availability were important predictors of vascular plant species richness. Mosses and liverworts responded to the availability of specific substrates (stones and topographic hollows), but were also affected by soil C:N. Overall, assemblages of mosses and vascular plants exhibited many similarities in how they responded to hydrological gradients, whereas the patterns of liverworts differed from the other two groups.

Carbon and charcoal

(Deluca 2012) Process models allow us to predict soil organic C losses but we presently lack a clear understanding of all the processes involved in forest soil C dynamics. Currently, this incomplete understanding of forest soil C dynamics and linkages to other cycles and responses to different disturbances all contribute to what we consider an over simplification of forest soil representation in models as a ‘C reservoir.’

Boreal forest ecosystems account for ∼50 per cent, or more, of world forest ecosystem C stocks. Soil C in boreal ecosystems has been reported to account for ∼85 per cent of the total biome C (Malhi et al., 1999) BUT taken from (Deluca 2012). Of the soil carbon, peatlands, although covering a small area (sweden 10-15%), account for probably more than 60 per cent while uplands account for the rest (my calcs). UPLANDS: Total ecosystem C storage in boreal forests varies by age, structure and stand history, all of which have a great influence on total C storage as reflected by changes in forest biomass, coarse woody debris, forest floor, and to a lesser extent, mineral soil. Mineral soil C (to 1.0 m depth) remains relatively stable and accounts for the majority of total ecosystem C across forest maturity and disturbance regimes. (Deluca 2012).

(Olsson 2009) that 60% of soil carbon is stored in the mineral soil for podzols. In general they found, the correlation coefficients for the linear relationship between SOC stock and site characteristics to be highest for N deposition, which explained up to 25% of variation, and latitude, which explained up to 20% of variation. Altitude had the lowest degree of explanation.

(Seedre 2011) Across much of the boreal, fire functions as a fundamental disturbance process that consumes the understory and moss bottom layer along with a portion of the humus pool and with a significant portion of the total C stored in the O horizon (Kasischke and Stocks, 2000) and partially resets the successional clock (Engelmark, 1999) with mineral soil C remaining greatly unchanged.

(Kelly 2016)used charcoal reconstructions of fire in Alaskan boreal forest to drive model simulations of carbon dynamics from AD 850–2006 and finds that fire was likely the dominant source of carbon-stock variability (accounting for 84 % of C stock variability) in boreal forests and that a recent increase in fire frequency since 1950 has led to large carbon losses.

Charcoal is formed by the incomplete oxidation of organic matter heated to temperatures that drive off volatile elements such as N, S and O, resulting in increased carbon density of the remaining organic matter (Demirbas 2008).

(González-Pérez 2004) “identify the following main effects of fire on soil organic matter: (I) general removal of external oxygen groups that yields materials with comparatively reduced solubility; (ii) reduction of the chain length of alkyl compounds, such as alkanes, fatty acids, and alcohols; (iii) aromatisation of sugars and lipids; (iv) formation of heterocyclic N compounds; (v) macromo-lecular condensation of humic substanc; and (vi) production of an almost unalterable component, the so called black carbon.”

(Johnson 2001) Meta-analysis: “it is clear that fire need not necessarily lead to a loss of soil C or N and indeed may cause increases in soil C and N by incorporation of charcoal and hydrophobic organic matter or by the invasion of N-fixing vegetation.”

(Hart 2013) Charchoal amounts of 12.5-340 g C m-2 are reported for boreal ecosystems Stand-specific factors (fire intensity, vegetation type and burning efficiency) probably play a much larger role in determining charcoal levels than time since formation. Rosengren (2000) found higher charcoal quantities in Scandinavian forest stands subject to more intense fires, the result of more biomass on more productive sites, where more biomass was consumed, compared with stands of low-intensity ground fires, consuming smaller amounts of biomass.

(Deluca 2012) Approximately 10 per cent of the woody biomass consumed by fire is converted to charcoal, a uniquely stable form of C with mean residence times measured in thousands of years (Figure 4) as opposed to months for twigs and small stems (DeLuca 2008). This stable form of C is often not accounted for when evaluating the influence of fire on total C storage in soil ecosystems. Interestingly, charcoal commonly accounts for app