The critical amplifying role of increasing atmospheric moisture demand on tree mortality and associated regional die-off.

Drought-induced tree mortality, including large-scale die-off events and increases in background rates of mortality, is a global phenomenon (Allen et al., 2010) that can directly impact numerous earth system properties and ecosystem goods and services (Adams et al., 2010; Breshears et al., 2011; Anderegg et al., 2013). Tree mortality is particularly of concern because of the likelihood that it will increase in frequency and extent with climate change (McDowell et al., 2008, 2011; Adams et al., 2009; McDowell, 2011; Williams et al., 2013). Recent plant science advances related to drought have focused on understanding the physiological mechanisms that not only affect plant growth and associated carbon metabolism, but also the more challenging issue of predicting plant mortality thresholds (McDowell et al., 2013). Although some advances related to mechanisms of mortality have been made and have increased emphasis on interrelationships between carbon metabolism and plant hydraulics (McDowell et al., 2011), notably few studies have specifically evaluated effects of increasing atmospheric demand for moisture (i.e., vapour pressure deficit; VPD) on rates of tree death. In this opinion article we highlight the importance of considering the key risks of future large-scale tree die-off and other mortality events arising from increased VPD. Here we focus on mortality of trees, but our point about the importance of VPD is also relevant to other vascular plants.

Much research discussion has stemmed from speculation that warmer temperatures and implicit increases in VPD exacerbated a recent widespread dieoff event of one tree species, Pinus edulis, in the southwestern USA (Breshears et al., 2005). This speculation was subsequently supported by theoretical developments regarding related processes (McDowell et al., 2008; McDowell, 2011), a controlled experiment (Adams et al., 2009), and regional empirical and modeling analyses (Weiss et al., 2012; Jiang et al., 2013; Williams et al., 2013). Numerous other studies reached similar conclusions for other systems (e.g., Allison et al., 2009; van Mantgem et al., 2009; Arora et al., 2013; Jiang et al., 2013; Liu et al., 2013). From a variety of approaches, these studies collectively concluded that rising temperature and associated VPD drive accelerating rates of mortality during drought. Although the effects of warmer temperature are receiving increased attention, effects of changes in VPD per se have been explicitly considered far less.

To focus on VPD, we return to fundamental relationships. Rising global surface temperature will curvilinearly increase saturation vapour pressure because warming increases the evaporation-to-condensation ratio, causing the gaseous phase of water to be increasingly favored (Bohren and Albrecht, 1998). VPD is the difference between the saturation vapour pressure and actual vapour pressure. While increased temperature is often accompanied by increased vapour pressure due to enhanced evaporation rates, increases in saturation vapour pressure outpace increases in actual vapour pressure as long as relative humidity is less than 100%, resulting in a curvilinear increase in VPD (Figure 1A). Consequently as global climate warms, VPD increases even though specific humidity is projected to increase in most regions (Held and Soden, 2006). Drought induces an additional positive feedback on VPD due to an increase in the ratio of sensible to latent heat fluxes caused by reduced transpiration and evaporation, thus causing a further rise in surface temperature and hence VPD (Maness et al., 2013).

Figure 1

A conceptual figure illustrating the effect of increased VPD on the biophysical factors that influence tree physiology, drought stress, and survival. Higher temperatures increase VPD non-linearly (A), higher VPD will generally both deplete soil moisture (B) and increase plant stress though changes in transpiration [C; based on data from Eamus et al. (2008)], all of which are projected to contribute to non-linear increases in forest stress [highlighted by the Forest Drought Severity Index (FDSI), with more negative values corresponding to increased stress] and resultant widespread regional mortality (D; Williams et al., 2013).

Climate-model projections of rapidly increasing VPD globally may cause pronounced levels of tree stress that may be unprecedented relative to what modern forests have evolved under, and for which landscape management strategies have been designed (e.g., Williams et al., 2013). If such stresses trigger associated widespread mortality, they then also have major impacts on landscape albedo and hence energy partitioning, biogeochemical cycling, regional carbon and water budgets, and the provisioning of ecosystem services (Adams et al., 2010; Breshears et al., 2011; Anderegg et al., 2013). Importantly, warmer temperatures and associated increases in VPD are two of the most pronounced climate change trends of recent decades and may be the climatic parameters that we can project with greatest confidence (IPCC, 2007). Therefore the need to understand the effects of increased VPD and temperature on forest stress and associated mortality is clearly apparent.

An increase in VPD affects both soil evaporation and plant physiology. Soil evaporation is affected by physical relationships with increased VPD under warmer temperature via Fick's law: E = g (VPD), where g is conductance of the surface boundary layer (Figure 1B). This causes increased rates of potential water loss from soils, thus reducing the amount of plant available water, which in turn could exacerbate plant water stress and associated mortality risk. In addition to this effect on soil evaporation, VPD affects plant physiology directly through its impact on stomatal closure and associated impacts on photosynthesis and carbon metabolism [Figure 1C; example data from Eamus et al. (2008)], transpiration rate increases with VPD up to a point (after which it remains high even if decreasing somewhat with VPD), the net result of which is likely a further exacerbation of plant water stress. As VPD rises, a series of physiological mechanisms may occur by which stomata close to maintain water tension within the xylem below a critical threshold (Tardieu and Simonneau, 1998). Such stomatal closure causes a reduction or cessation of photosynthesis, but failure to close stomata may cause desiccation through excessive water loss. These relationships were the basis for the carbon starvation and hydraulic failure hypotheses (McDowell et al., 2008, 2011): a reduction in photosynthesis, if prolonged and severe, should cause a decline in photosynthate available to drive metabolism and defense against biotic agents. Alternatively, if stomata remain relatively open during periods of elevated VPD, this may allow maintenance of positive photosynthetic rates, but may allow transpiration to exceed critical rates causing xylem cavitation—the formation of embolized vessels through the entry and expansion of air bubbles that block water transport (Tyree and Sperry, 1989; Thomas and Eamus, 1999). If embolized conduits remain un-repaired, this can lead to hydraulic failure, or dehydration and subsequent mortality (McDowell et al., 2008). Carbon starvation and hydraulic failure are likely interactive in driving mortality through multiple pathways (see Box 2, Figure 1 in McDowell et al., 2011), as supported by recent work for several species (Anderegg et al., 2012; Adams et al., 2013; Galvez et al., 2013; Quirk et al., 2013; Sevanto et al., 2013). Increased VPD can both increase xylem tensions that lead to hydraulic failure and inhibit phloem function, limiting the mobility of carbohydrate resources to sink tissues, potentially exacerbating carbon starvation and preventing xylem embolism repair (McDowell et al., 2011).

Note that the VPD effects on physiology described above do not negate the direct negative impact rising temperature alone can have on plant survival. Although growth respiration is reduced during drought (Amthor and McCree, 1990; Körner, 2003; McDowell, 2011), the increased temperatures associated with higher VPD may increase maintenance respiration, potentially accelerating carbon starvation (Adams et al., 2009). Further, rising temperature may also increase the speed to reproductive maturation of biotic agents such as bark beetles, thus increasing the rate of biotic attack on vegetation (Raffa et al., 2008). Recent modeling analysis disaggregated the effects of VPD and temperature on tree physiology in Eucalyptus (Eamus et al., 2013) and demonstrated that increased VPD (+1.0 or +2.5 kPa above controls) should have a much larger impact on tree health (defined as a prolonged loss of NPP, Net Primary Productivity) than increased temperature (+2.0 or +5.0 °C above controls). Similarly, in an experimental study, increased VPD associated with higher temperature led to greater transpiration and faster mortality during drought for tree seedlings common to the Great Plains forest-grassland ecotone of the central United States (Will et al., 2013). These modeling and experimental results are consistent with recent studies relating spatial patterns in VPD anomalies to tree die-off (Weiss et al., 2009, 2012). Additionally, powerful new relationships detected among regional tree growth, mortality and warm-season VPD portend non-linear increases in forest stress and associated tree mortality in the future (Figure 1D, as reflected in the Forest Drought Severity Index, FDSI, that includes a term for atmospheric demand; Williams et al., 2013) Collectively the physical (Figures 1A,B) and physiological (Figure 1C) effects of VPD are expected to contribute to greater water loss rates from the system and associated increases in tree drought stress and associated mortality.

The fundamental fine-scale relationships of increased temperature and associated increased VPD have profound global-scale implications for the future distributions of vegetation. VPD and temperature are core constituents of the three principle climatic determinants of the distributional patterns of vegetation, as exemplified in the Holdridge (1967) life-zone classification scheme: temperature, rainfall and potential evapotranspiration (the latter of which is strongly dependent on VPD). The potential for major redistribution of ecosystem boundaries following changes in evaporative demand without concomitant changes in rainfall is exemplified by the southern boundaries of boreal forest and aspen parkland in Canada, which correspond most closely with climatic (rainfall and atmospheric water content) moisture regimes (annual precipitation minus potential evaporation; Hogg, 1994). In general, there is a paucity of mortality experiments that manipulate either temperature or VPD, let alone both independently, and the former of these have mostly been limited to Pinus and Eucalyptus. Needed to compliment more mechanistic approaches are also experimentally determined climate-mortality envelopes that are specific to drought-induced tree mortality. Although much uncertainty remains about the specifics of the mechanisms underlying mortality, our principle point is that the risk posed by intensifying atmospheric moisture demands to future tree mortality and associated die-off events remains a critical but little-studied aspect in this domain. Additional study is required if we are to effectively predict and manage the consequences of future climate change and tree mortality. In summary, we need to shift focus to the critical amplifying role of VPD, not just of associated temperature, in driving tree mortality during drought because VPD changes impose fundamental curvilinear physical and physiological responses. Importantly climate models consistently predict VPD as well as temperature to increase in the future and these trends will almost certainly increase forest stress, tree mortality, and associated large-scale tree die-off events in many regions globally.