The oxygen stable isotope composition of plant organic matter (OM) (particularly of wood and cellulose in the tree ring archive) is valuable in studies of plant–climate interaction, but there is a lack of information on the transfer of the isotope signal from the leaf to heterotrophic tissues.
We studied the oxygen isotopic composition and its enrichment above source water of leaf water over diel courses in five tree species covering a broad range of life forms. We tracked the transfer of the isotopic signal to leaf water-soluble OM and further to phloem-transported OM.
Observed leaf water evaporative enrichment was consistent with values predicted from mechanistic models taking into account nonsteady-state conditions. While leaf water-soluble OM showed the expected 18O enrichment in all species, phloem sugars were less enriched than expected from leaf water enrichment in Scots pine (Pinus sylvestris), European larch (Larix decidua) and Alpine ash (Eucalyptus delegatensis).
Oxygen atom exchange with nonenriched water during phloem loading and transport, as well as a significant contribution of assimilates from bark photosynthesis, can explain these phloem 18O enrichment patterns. Our results indicate species-specific uncoupling between the leaf water and the OM oxygen isotope signal, which is important for the interpretation of tree ring data.
Plant physiological responses to climatic and weather conditions in the past and at present are critical to understanding the impact of global climate change on ecosystem performance and resilience in the future (McDowell et al., 2008; Sternberg, 2009). Evaporative enrichment of 18O (Δ18O) in leaf water and subsequent 18O enrichment of assimilates can be used to characterize environmental and physiological factors that control transpiration, based on established mechanistic models (Craig & Gordon, 1965; Dongmann et al., 1974; Farquhar & Cernusak, 2005). The oxygen isotopic composition of tree rings as archives has been used to explore long-term precipitation patterns (Treydte et al., 2006), seasonality of precipitation (Saurer et al., 2002), tree responses to variations in atmospheric water demand and soil water availability (Barbour et al., 2002; Roden et al., 2005) and intra-annual patterns of transpiration rates (Gessler et al., 2009a).
The oxygen isotopic composition (δ18O) in leaf water reflects both δ18O of source water and the evaporative conditions in the leaf–atmosphere continuum (Dongmann et al., 1974; Roden & Ehleringer, 1999b; Barbour et al., 2004). During transpiration, the water isotopologues containing the lighter 16O isotope escape from liquid into vapour faster and diffuse faster than the heavier ones, thereby enriching the water in 18O at the sites of evaporation. This evaporative enrichment of water is governed by the bidirectional exchange of water vapour between the leaf and the ambient air, and so is affected by the vapour pressure deficit of the air and the isotopic composition of the water vapour (Craig & Gordon, 1965).
Isotopic composition of water in the mesophyll cells of the leaf lamina is influenced by the evaporative enrichment at the sites of evaporation. Lamina leaf water consists of a mixture of nonenriched xylem (source) water and water from the sites of evaporation (Farquhar & Lloyd, 1993). Newly produced assimilates are assumed to carry the signature of the lamina leaf water at the time when they were produced with an equilibrium fractionation factor (εwc) resulting in carbonyl oxygen being 25–28‰ more enriched than the lamina water (Sternberg & Deniro, 1983; Yakir & Deniro, 1990). Barbour & Farquhar (2000) assume that sucrose, as the main leaf exported sugar, is in full isotopic equilibrium with cytoplasmic water and thus should carry the isotope signature of mean lamina leaf water plus εwc. The often cited value of 27‰ for εwc (Barbour & Farquhar, 2000; Cernusak et al., 2003) is an average value of the difference in the 18O isotopic composition between the cellulose of different aquatic plants and tunicates and the water in which they grew (DeNiro & Epstein, 1981). A comparable enrichment of leaf cellulose above leaf water was also found for different nonwoody terrestrial plants (DeNiro & Epstein, 1979; Helliker & Ehleringer, 2002; Cernusak et al., 2003). The situation is more complex in nonleaf tissues including tree rings, which can serve as long term, dateable, archives for isotopic information. Cellulose in tree rings is affected by both the isotopic composition of leaf water, and the sugars produced therein, and the isotopic composition of the xylem water, which equals source water (Roden et al., 2000). This is because some of the oxygen atoms of the phloem-originating sucrose are assumed to be exchanged in the trunk with nonenriched xylem water during cellulose synthesis (Sternberg et al., 1986; Farquhar et al., 1998; Roden & Ehleringer, 1999a; Barbour, 2007). When averaged over a large number of species, 42% of the organic oxygen seems to be exchanged (Cernusak et al., 2005). However, discussion continues as to whether this exchange rate varies over the growing season or over longer time periods (Gessler et al., 2009a), or if it is rather unaffected by environmental conditions (Sternberg & Ellsworth, 2011).
Only recently, it was assumed that organic compounds transported in the phloem might be subjected to seasonally variable exchange with source water resulting in a partial uncoupling of the leaf water signal already on its way to the tree ring (Offermann et al., 2011). In agreement with this finding, Barnard et al. (2007) observed an 18O depletion of phloem organic matter (OM) compared to the values expected from leaf water enrichment. Because the phloem sugars convey the leaf water isotopic signal to the tree rings, a deeper understanding of the processes and mechanisms affecting phloem δ18O is crucial for the interpretation of the oxygen isotope composition tree ring archive as well as for the quantification of oxygen atom exchange during cellulose synthesis.
Exchange between water and organic oxygen in carbonyl groups can occur under normal physiological conditions (Sternberg et al., 1986) but exchange does not occur for other oxygen-containing functional groups such as hydroxyl or carboxyl groups (Barbour, 2007). The type of compounds transported in the phloem (Van Bel & Gamalei, 1992; Van Bel, 1993; van Bel & Hess, 2008) might strongly affect the overall δ18O of phloem OM (c.f. Schmidt et al., 2001) and also the oxygen isotope composition of tree ring tissue.
Measurements of δ18O in phloem OM and a comparison with lamina leaf water, and recently assimilated and leaf-exported OM are scarce (for an overview see Gessler et al., 2009a), and hence we examined three different angiosperm and two gymnosperm tree species covering a broad range of tree life forms: (1) angiosperm, broadleaf, deciduous – sessile oak (Quercus petraea), European beech (Fagus sylvatica); (2) angiosperm, broadleaf, evergreen – Alpine ash (Eucalyptus delegatensis); (3) gymnosperm, coniferous, evergreen – Scots pine (Pinus sylvestris); (4) gymnosperm, coniferous, deciduous – European larch (Larix decidua). We carried out experiments over diel or diurnal courses to address the following questions: (1) Does the oxygen isotope enrichment of leaf sugars and phloem-transported assimilates generally reflect lamina leaf water enrichment in all species? (2) If not, can differences among species be attributed to the chemical composition of phloem-transported compounds or (3) are differences related to leaf/canopy morphological (e.g. needles vs broadleaves) or physiological traits? To answer these questions we measured and modelled (lamina) leaf water 18O enrichment over the diel course and related these values to water-soluble leaf OM (as a proxy for leaf sugars) and phloem-transported OM. In addition, we determined the phloem metabolome in oak, beech and pine to account for possible differences in the organic compounds metabolized between species and their contribution to the phloem 18O signature.
The questions we raise here are highly relevant to studies that use the δ18O of plant OM for physiological or climatic insights. δ18O of plant organic material can only provide an integrative tool to study the evaporative and photosynthetic processes that drive or are associated with plant water fluxes (Werner et al., 2012) if δ18O in phloem OM reflects the oxygen isotopic signature of leaf water or if changes in δ18O during phloem loading and/or transport can be accounted for. Moreover, if phloem OM δ18O does not directly reflect the leaf water oxygen isotope signature, interpretation of tree ring δ18O data would need to be reconsidered as cellulose is produced from the phloem-transported sugars.
Materials and Methods
Experiments were performed at four different sites (Hartheim (Pinus sylvestris L.), Hesse II (Fagus sylvatica L. and Quercus petraea (Matt.) Liebl.), Tumbarumba (Eucalyptus delegatensis R. T. Baker) and Lötschental (Larix decidua Mill.)) throughout Europe and Australia. The main site characteristics are given in Table 1. Additional detailed information on the sites can by found in Holst et al. (2008; Hartheim), Granier et al. (2000; Hesse), Gessler et al. (2007a; Tumbarumba) and Moser et al. (2010; Lötschental).
Table 1. Main characteristics of the four experimental sites
Altitude (m asl)
Target tree species
Tree height (m)
Tree age (yr)
Stand density (trees ha−1)
Target tree species: species measured and sampled for isotope analyses. In Hesse II two species were examined. Tair, long-term mean annual air temperature; average daily temperatures are given for Hartheim and Hesse, average daily maximum (max) and minimum (min) temperatures are given for Tumbarumba. For this site Tair was measured at a 40 km distance from the flux station and at an elevation of 750 m. Precip, annual sum of precipitation; for Hartheim and Hesse long-term average sums are given, for Tumbarumba the average sum of the years 2002–2004 is shown. LAI, leaf area index; nd, not determined.
At the Lötschental site two stands located at two altitudes, one at the upper tree line of a south-facing slope and the other at the valley bottom on a rocky hill were examined. During the 2008 growing season, the mean temperature was 11.6°C at the valley bottom and 8.3°C at the treeline. Hydrological conditions are generally drier at the valley site due to lower precipitation (292 mm vs 410 mm; week 25–42).
Air temperature (Ta), vapour pressure deficit (VPD) and photosynthetically active radiation (PAR) were determined above the canopy at the Hartheim, Hesse II and Tumbarumba sites. For details of the instrumentation see Holst et al. (2008), Granier et al. (2000) and Leuning et al. (2005), respectively. At the Lötschental sites, the meteorological parameters were determined 2 m above ground in open patches close to the trees examined. All data are averages over a 30-min period.
Experimental set up and sampling of plant material
The measurement campaign (P. sylvestris) took place on 19.ix.2005 (first sampling: 10:00 h) and 20.ix.2005 (last sampling: 13:30 h) on three dominant trees growing close to a scaffold tower. Needles and twigs were sampled and gas exchange measurements performed in the sun-exposed part of the upper crown of the trees every 4 h (with the exception of the last sampling round which was started half an hour earlier). Needles were separated into current and previous year needles. We determined bulk leaf water 18O evaporative enrichment for both current and previous year needles separately once during the night (02:00 h) and once during the day (14:00 h). The measured values were not significantly different between the two needle age classes (P <0.05; n =3) at either time. As a consequence, both age classes were bulked for further analyses of the isotopic composition of leaf water and OM.
The measurements in Hesse were performed between 26.ix.2005 and 27.ix.2005. In total, eight sampling/measurement rounds were performed for both tree species (F. sylvatica and Q. petraea) starting at 11:30 h and terminating at 14:00 h on the following day. Using scaffolding, the leaves and twigs from the upper sun crown of three representative trees per species were harvested and at the same time gas exchange was determined.
The measurements were carried out between 9.iii.2005 and 10.iii.2005. Five measurement rounds were performed starting at 08:30 h and terminating at 08:00 h on the following day. We selected three representative dominant individuals of E. delegatensis with a maximum height of c. 38 m. The canopy of the trees was accessed for leaf and twig sampling as well as for gas exchange measurements using a 40-m hydraulic lift installed on a truck.
At both sites (valley and treeline) we selected four representative L. decidua trees. The measurement campaigns at the valley bottom were performed on 10.vi.2008 and 14.vii.2008. At the treeline one campaign was carried out on 18.viii.2008. The stands were quite open, so that even the lowest branches (which could be accessed from the ground) of all individuals were exposed to direct sunlight. From these lower branches needles and twigs were harvested seven times during the light period starting at 06:00 h in June and at 07:00 h at the two other dates. From the twigs we collected phloem exudates as well as xylem water.
Extraction of leaf water, xylem water and OM fractions
Bulk leaf water
Needles of the current and recent year flush (P. sylvestris), current year needles (L. decidua) and leaves (F. sylvatica, Q. petraea and E. delegatensis) were quickly transferred into airtight closed glass tubes and frozen. Needle/leaf water was obtained by cryogenic vacuum extraction according to Ehleringer et al. (2000).
Twig xylem water of pine, oak, beech and Alpine ash was extracted from cut twigs by applying a gentle vacuum following Brandes et al. (2007). For larch the xylem water was extracted from the woody tissue of twigs by cryogenic vacuum extraction. Brandes et al. (2007) showed that both methods result in comparable values for xylem water δ18O.
For all five species, bark pieces removed from the twigs were placed into 1.8-ml deionized water volumes according to the procedure described by Gessler et al. (2004) avoiding contamination of the phloem exudates by cellular constituents (Schneider et al., 1996). We refer to the OM fraction obtained with this exudation procedure described above as bulk phloem OM. In a further step the exudates of pine, oak and beech were passed through Dowex-50 (H+) and Dowex-1 (Cl−) columns in series to separate neutral sugars from amino acids and organic acids as described by Richter et al. (2009). The eluate collected is referred to as neutral phloem sugars.
For beech and pine we tested whether the exchange of oxygen atoms occurred between bulk phloem OM and the exudation solution as done previously by Offermann et al. (2011). For this purpose pairs of bark pieces were harvested in the direct vicinity of a given twig. One of these bark samples was incubated in relatively 18O depleted deionized water (δ18O: −8.9 ± 0.3‰) and the other one in relatively enriched water (δ18O: 8.9 ± 2.5‰). The oxygen isotope signatures of bulk phloem OM did not differ between the two exudation solutions (beech: δ18O of bulk phloem OM exuded in enriched water: 28.5 ± 1.1‰ and in depleted water: 28.4 ± 0.9‰ (n =11); pine: δ18O in enriched water: 30.1 ± 0.8‰ and in depleted water: 30.3 ± 1.2‰ (n =10)). We thus can exclude any oxygen atom exchange during the exudation procedure.
Leaf water-soluble OM
For all five species water-soluble OM was extracted from the leaves and needles according to a modification of the method described by Gessler et al. (2009b). Frozen leaf material was denatured in a microwave oven for 1 min and dried at 50–60°C. Leaves were ground with a ball mill (MM 200; Retsch GmbH, Haan, Germany). Aliquots of 50–70 mg were extracted in 1.5 ml deionized water on a shaker for 1 h at 4°C and subsequently put in a water bath at 95°C for 1 min for denaturation of soluble proteins. After cooling on ice, samples were centrifuged at 4°C and 12 000 g for 10 min. Supernatants were stored at −20°C until further analysis.
Collection of water vapour
At the Hartheim, Hesse II and Tumbarumba sites atmospheric water vapour was collected during the day between 13:00 and 14:00 h and during the night between 02:00 and 03:00 h by cryogenic condensation from middle canopy height. The air was pumped through tubing at a flow rate of c. 1 l min−1 and through a glass u-tube inserted in a dewar containing an ethanol – dry ice slush at −70 to −80°C. Water vapour was collected in a cold trap for 1–2 h and kept frozen until δ18O analysis. We averaged the daytime and night-time values, giving mean values of −17.9‰, −15.2‰ and −17.6‰ for Hartheim, Hesse II and Tumbarumba, respectively.
Gas exchange measurements
Leaf gas exchange of beech, oak, Alpine ash and pine was measured in the upper sun-exposed canopy in the direct vicinity of the twigs sampled for isotope analysis. For the three broadleaf species three leaves were measured per individual tree with a broadleaf chamber connected to a portable gas exchange system (LI-COR 6400: Li-Cor Biosciences, Lincoln, NE, USA; or GFS3000: Heinz Walz GmbH, Effeltrich, Germany). For pine, small twigs (with their needles attached) were inserted into a conifer leaf chamber attached to the same gas exchange system. All measurements were conducted under ambient light and temperature conditions. Pine twigs with previous and current year needles attached were placed in the gas exchange chamber. In accordance with the results of Beadle et al. (1985) we assumed gas exchange and stomatal conductance of the age classes to be equal at that time of the year. For all four species net CO2 and H2O exchange rates were measured, and stomatal conductance (gs) was subsequently calculated according to von Caemmerer & Farquhar (1981). The temperature of beech and oak leaves was determined with a thermocouple; for pine needles the temperature was assumed to be equal to ambient air temperature as suggested by Walcroft et al. (1997), because needles are thought to be strongly coupled with the environment. The leaf area of the needles inserted into the chamber was determined according to Barnard et al. (2007).
The determination of δ18O in water and OM samples was performed using a TC/EA high temperature conversion/elemental analyser coupled to either a DeltaPlus XP (ThermoFisher, Bremen, Germany) or an Isoprime (Micromass, Middlewich, UK) mass spectrometer. The precision was < 0.17‰. The oxygen stable isotope composition is expressed using small delta notation in parts per thousand, relative to the international Vienna Standard Mean Ocean Water (VSMOW) standard.
Bulk leaf water, cryogenically trapped water vapour and xylem water
Water samples of 0.7 μl were injected into the TC/EA. Each sample was analysed four times in sequence and only the value of the last measurement was taken into account to avoid memory effects.
Phloem bulk OM, phloem neutral sugars and leaf water-soluble OM
Samples of 40–100 μl of the phloem exudation solution or of the leaf extracts were transferred to silver capsules and water was evaporated at 60°C in an oven. The samples contained on average c. 300 μg organic O.
Isotopic calculation and modelling
The oxygen isotope enrichment of bulk leaf water or plant OM (leaf water-soluble OM, bulk phloem OM, neutral phloem sugars) is expressed as enrichment above source water (Δ18O):
(δ18Op, oxygen isotopic composition of leaf water or plant OM; δ18Osw, isotopic composition of the source water). In our case we calculated the 18O enrichment based on xylem water as source water.
According to Farquhar & Gan (2003), the 18O enrichment of bulk leaf water is given by:
(φx, φv and φL, proportions of total water associated with the longitudinal xylem, the veinlets and the lamina mesophyll, respectively; Δ18Ox, Δ18Ov and Δ18OL, evaporative enrichment of xylem, veinlet and lamina leaf water above source water, respectively). Lamina leaf water is the reaction water in which assimilates are produced, and thus it is necessary to estimate Δ18OL from measured Δ18OB. Following Farquhar & Gan (2003), we assumed the water volume in the veinlets to be negligible. Because we excluded the main veins from the leaf sample of beech and oak, we assumed for these two species that mesophyll water composition was equivalent to the isotopic composition of extracted bulk leaf water. For the coniferous species and for Alpine ash we applied the procedure described in detail by Barnard et al. (2007) to estimate φx. Lin et al. (2001) showed that the contribution of xylem to the cross-sectional area of current year Scots pine needles (sampled in October) was 2.2%. A comparable xylem contribution of 3% has been observed for larch (Takemoto & Greenwood, 1993). From cross-sectional cuttings of leaf samples from E. delegatensis we estimated the main vein to contribute to 10% of the leaf water volume. From these xylem areas, φx values were calculated following Barnard et al. (2007) and Δ18OL was estimated from Δ18OB. For needles we assumed leaf vein xylem water not to be enriched in 18O, for E. delegatensis we determined major vein water to be enriched by 2.8‰ above source water.
Leaf water enrichment during measurement campaigns was modelled with approaches of increasing complexity as described in detail by Barnard et al. (2007) for pine, oak, beech and Alpine ash. We calculated the isotopic enrichment of 18O over source water at the site of evaporation in the leaf (Δ18Oes) under steady-state conditions and lamina leaf water enrichment under steady-state (Δ18OLs) and nonsteady-state conditions (Δ18OLn). Details are given in the Supporting Information Notes S1.
For pine and Alpine ash we additionally modelled Δ18OLs for the 2 d before gas exchange measurements and leaf and phloem sampling were performed. For these 2 d we calculated stomatal conductance and transpiration based on their relationship with VPD determined during the measurement campaigns. Leaf temperature was assumed to equal air temperature and the scaled effective path length for water movement from the xylem to the site of evaporation (L) was assumed not to be different from the value determined during the measurement period.
In order to calculate mean daytime oxygen isotope enrichment of leaf water and phloem OM above twig xylem water (weighted Δ18O) for pine, oak, beech and Alpine ash, the Δ18O values (see Eqn 1) of each daytime measurement time were weighted by the corresponding CO2 assimilation rate measured (A, mol m−2 s−1), according to Cernusak et al. (2005):
(numerator, daily (daytime) integral of the product of A and Δ18O (‰ mol m−2); denominator, daily integral of A (mol m−2)). No gas exchange measurements were performed with larch, so we weighted measured leaf water Δ18O values by the half-hourly averages of photosynthetic active radiation before harvest as a rough proxy for photosynthesis. We also weighted modelled Δ18OLs of pine and ash from the 2 d preceding the gas exchange measurements. To obtain A values for this time period (when no gas exchange measurements were performed) we calculated a photosynthesis–light response curve for the gas exchange measurement period and calculated A from photosynthetically active radiation.
Phloem metabolite analysis
Samples (250 μl) of the bulk phloem exudate of pine, oak and beech were dried under vacuum and derivatisation (methoxyamine and silylation with N-methyl-N-trimethylsilylfluoroacetamide) as well as GC-MS analysis for metabolite profiling were performed without further purification according to Erxleben et al. (2011). The derivatised phloem samples were injected into a GC-quadrupole MS system (GC: 7890A; MS: 5975C; Agilent Technologies, Waldbronn, Germany) operating in electron impact ionization. Data were deconvoluted and peak areas quantified using the AMDIS software (http://chemdata.nist.gov/mass-spc/amdis/). Peak identifications were carried out by matching retention indices and mass spectral similarity against the NIST 05 mass spectral library (http://www.nist.gov/srd/nist1a.cfm) and a user-defined metabolite library based on the Golm metabolome database ((Kopka et al., 2005); http://csbdb.mpimp-golm.mpg.de/csbdb/gmd/msri/gmd_msri.html). For the 25 most abundant identified compounds calibration curves were made with external standards to quantify metabolite concentrations.
All statistical analyses were performed using NCSS 2004 (Number Cruncher Statistical Software, Kaysville, UT, USA). Differences in εwc between different OM pools were determined using analysis of variance (GLM-ANOVA). Regression lines between ∆18O values of leaf and phloem OM pools were determined by linear regression analysis.
Environmental parameters at the field sites
In Hesse II, the highest air temperature during the measurement campaign was 19.1°C (Fig. 1a). VPD varied between 1.6 and 8.7 hPa. Maximum daytime temperatures were 22°C during the 2 d before the campaign and were thus higher than during the measurements. Day-to-night differences in VPD and maximum VPD values were also greater on the days preceding the sampling. At the Hartheim site (Fig. 1b) the maximum air temperature during the measurement campaign was 17.3°C. VPD ranged from 0.1 to 9.7 hPa during that period. VPD and air temperature values were comparable during the 2 d preceding the measurement campaign with the exception of higher minimum night-time temperatures between 17 and 19.ix.2005. At Tumbarumba the highest air temperature during the measurement campaign was 14.8°C and VPD reached 12.5 hPa (Fig. 1c). Somewhat lower maximum and minimum VPD and air temperature values were observed during the 2 d before the campaign. At the Lötschental valley site, the temperature range during the June measurement campaign was between 6.4 and 17.9°C and VPD reached a maximum of 9.2 and a minimum of 0.9 hPa (Fig. 1d). Both maximum temperatures and maximum VPD were slightly lower during the preceding 2 d, whereas minimum values of both, temperature and VPD were comparable among diel courses. During the July campaign at the Lötschental valley site the VPD range was 0.3–8.1 hPa and the temperature range 6.8–13.6°C (Fig. 1e). The maximum air temperature was comparable on the preceding day but rose to 16.6°C 2 d before the campaign. The maximum VPD was 3.2 and 1.2 hPa on 12 and 13.vii.2008, respectively. At the Lötschental treeline site VPD varied between 3.4 and 10.0 hPa on the measurement day (Fig 1f). The minimum temperature during sampling was 8.4°C and a maximum of 15.8°C was reached in the afternoon. Both temperature and VPD were lower during the two preceding days, reaching maximum values of 4.8 hPa and 10.4°C, respectively.
Leaf water evaporative enrichment - observed and modelled values
In beech (Fig. 2a) and oak (Fig. 2b) leaf water 18O enrichment (Δ18OL) showed comparable diel courses with maximum values after midday and a minimum before sunrise at 06:00 h. The observed range of Δ18OL was between 4.0‰ and 11.3‰ for beech and between 3.6‰ and 8.9‰ for oak. This enrichment was slightly higher with pine (Fig. 2c). The diel pattern was time-shifted in pine, with the maximum Δ18OL being observed in the late afternoon at 18:00 h and the minimum after sunrise at 10:00 h. In Alpine ash, the highest leaf water 18O enrichment was observed in the afternoon and during the first part of the night (Fig. 2d). For all four species, daytime values of measured Δ18OL were consistently lower than calculated Δ18Oes. The scaled effective path length (L) that was used to calculate the Péclet number (Eqn S2) was estimated based on the discrepancy between the predicted Δ18Oes and observed Δ18OL at time points between 13:30 and 18:00 h, when Δ18OL was assumed to be at steady state. We calculated an L of 0.017, 0.021, 0.060 and 0.025 m for beech, pine, oak and mountain ash, respectively. While the predictions of mean lamina leaf water enrichment that assumed isotopic steady state (Δ18OLs) were in rather good agreement with the observed enrichment during the light period, they underestimated Δ18OL in beech, oak and pine during the night. In Alpine ash, both calculated Δ18Oes and Δ18OLs were higher than the observed values during the night, mainly due to the high night-time VPD during the measurement campaign (cf. Fig. 1c) The nonsteady-state model (Δ18OLn) finally predicted lamina leaf water evaporative enrichment adequately for the whole diel course in all four species (Fig. 2) with only a slight underestimation of night-time values for pine.
Transfer of leaf water 18O enrichment to recent assimilates
Newly produced assimilates carry the signature of the leaf water at the time when they are produced with an equilibrium fractionation factor (εwc) resulting in the carbonyl oxygen being c. 27‰ more enriched than leaf water (Sternberg & DeNiro, 1983; Yakir & DeNiro, 1990). As a consequence, we compared ∆18OL + 27‰ with Δ18O of bulk phloem and leaf water-soluble OM during the diel/diurnal course for beech (Fig. 3a), oak (Fig. 3b), pine (Fig. 3c), Alpine ash (Fig. 3d) and larch (Fig. 3e,f). For all five species it was obvious that the maximum variations in Δ18O of phloem OM (beech, 1.2‰; oak, 0.7‰; pine, 0.6‰; Alpine ash, 2.9‰; larch, 2.7‰) and of leaf water-soluble OM, which has a comparable range of variation, were much smaller than those of leaf water (beech, 7.3‰; oak, 5.3‰; pine, 6.1‰; Alpine ash, 7.4‰; larch, 13.4‰).
In the two broadleaf deciduous species, the Δ18O of bulk phloem OM was lower than or similar to ∆18OL + 27‰ at midday and in the afternoon and higher in the dark period and in the morning. In pine and Alpine ash, bulk phloem OM Δ18O was below ∆18OL + 27‰ during the whole diel course. For larch, where we only carried out measurements during the light period, bulk phloem OM 18O enrichment was higher than ∆18OL + 27‰ at the valley bottom in June and July (Fig. 3e) until 08:00 h in the morning, but fell below ∆18OL + 27‰ by up to 12.1‰ during the rest of the light period. At the tree line in August, Δ18O of bulk phloem OM of larch was lower than ∆18OL + 27‰ during the whole daytime measurement period (Fig. 3f). The average diel (day and night) bulk phloem Δ18O was 35.7, 34.1, 35.1, 31.2‰ in beech, oak, pine and Alpine ash, respectively. The average daily bulk phloem Δ18O in larch was between 31.7 and 33.4‰ depending on time point and site. Clearly Δ18O of leaf soluble OM was higher than that of bulk phloem OM in pine, Alpine ash and larch.
Photosynthesis-weighted daytime Δ18O of lamina leaf water was compared with the diel nonweighted or daytime-photosynthesis-weighted average of Δ18O of phloem OM for beech, oak, pine and Alpine ash (Table 2). For larch, the Δ18O of leaf water was weighted by photosynthetic active radiation as a proxy. In the two broadleaf deciduous species the difference between weighted Δ18OL and Δ18O phloem OM amounted to c. 27‰, independent of the averaging and weighting procedure for the phloem values. However, the difference for the two coniferous species and the evergreen broadleaf species was lower than 27‰, reaching values as low as 16.7‰ for larch trees growing at the tree line. The data from pine and Alpine ash show that these values were consistently low, independent of whether only daytime or day-plus-night averages for Δ18O of bulk phloem OM were used for the comparison. There was no difference in the 18O isotopic signature between phloem bulk OM and the phloem neutral OM fraction for the three species (beech, oak, pine) examined.
Table 2. Difference between leaf water evaporative enrichment and Δ18O in fast-turn over organic matter (OM) pools (εwc) in leaf and phloem
Beech (Fagus sylvatica)
Oak (Quercus petraea)
Pine (Pinus sylvestris)
Alpine ash (Eucalyptus delegatensis)
Larch (Larix decidua)
Observed daytime leaf water enrichment (‰) was weighted for photosynthesis (beech, oak, pine and Alpine ash) or photosynthetic active radiation (larch) and related to the nonweighted diel average of the OM pools with the exception of Phloem bulk OM*, where phloem OM values during the light period were also weighted for photosynthesis. Data shown are average values from three to four trees per species ± SD. Different letters indicate significant differences among the different OM fractions in a given species (at a given site/time point). nd, not determined.
Leaf water-soluble OM
27.2 ± 0.4a
26.7 ± 0.6a
25.5 ± 0.6a
26.8 ± 0.9a
26.3 ± 0.4a
25.7 ± 0.5a
Phloem bulk OM
27.0 ± 0.5a
26.7 ± 0.5a
23.5 ± 0.6b
22.2 ± 0.8b
22.0 ± 0.6b
18.5 ± 1.1b
16.7 ± 1.0
Phloem bulk OM*
27.2 ± 0.5a
26.7 ± 0.6a
23.5 ± 0.7b
22.2 ± 1.0b
Phloem neutral fraction
27.1 ± 0.4a
26.7 ± 0.5a
23.4 ± 0.7b
We might assume that turnover times for phloem OM are longer than those for leaf water and that consequently Δ18O of phloem OM might be influenced by leaf water enrichment from preceding days. Accordingly, we calculated Δ18OLs of pine and Alpine Ash for the light period (where it showed quite good agreement with measured leaf water values; cf. Fig. 2) for the 2 d before phloem sampling. For pine, photosynthesis-weighted Δ18OLs for the preceding 2 d was estimated to be 12.8‰ on average and was thus slightly higher than the weighted observed Δ18OL (11.4‰) during the sampling period. The difference between Δ18OLs from the two preceding days and the average Δ18O phloem OM during the sampling period amounted to 22.3‰, thus deviating by 4.7‰ from the theoretical values of 27‰. For Alpine ash, the calculated weighted Δ18OLs of the two preceding days was comparable (9.3‰) with measured Δ18OL (8.9‰) during the campaign. Thus, the difference between this modelled Δ18OLs and the measured Δ18O phloem OM was still clearly lower than the expected 27‰.
The comparison between values of leaf water-soluble OM and bulk phloem OM for all five species, and the comparison between Δ18O values of leaf water-soluble OM and the Δ18O of neutral phloem sugars for beech, oak and pine, are illustrated in Fig. 4. For the two broadleaf deciduous species (Fig. 4a,b), the Δ18O values of both bulk phloem OM and neutral phloem sugars were similar to leaf water-soluble OM during the whole diel course, as indicated by the points scattering around the 1 : 1 line. In contrast to beech and oak, the two phloem fractions in pine were both depleted on average by 2.0‰ compared to leaf water-soluble OM (Fig. 4c). For Alpine ash the bulk phloem fraction was on average depleted by 4.7‰ and for larch by 4.3‰ (June) and 7.2‰ (July) compared to leaf water-soluble OM.
Phloem metabolic profile
Different metabolites might have different 18O isotopic compositions and thus might be a source of variation in Δ18O phloem OM among species. In all three species examined sucrose contributed most to the organic oxygen in phloem OM (Fig. 5) making up 95% (beech), 93% (oak) or 89% (pine). Fructose and glucose together made up between 2.3% and 3.6% and raffinose, myo-inositol, malate and the sum of amino acids each contributed < 1% in each species. Cyclitols were present in the bulk phloem OM of oak and pine: Quercitol contributed 2.8% to organic oxygen in phloem OM in oak and pinitol 5.6% in pine.
Observed lamina leaf water Δ18O is consistent with values predicted from mechanistic models
The simplest evaporative enrichment model (Eqn S1) considers enrichment at the sites of evaporation only (Δ18Oes). The second model (Eqn S2) adds a Péclet effect (Δ18OLs) and the final model (Eqn S3) also takes into account leaf isotopic nonsteady-state conditions (Δ18OLn). In all four species examined it is obvious that daytime evaporative enrichment can only be adequately described when the transpiration-dependent mixing of 18O enriched water with nonenriched xylem water is taken into account. Thus Δ18Oes overestimated the actual values of Δ18OL during the day, when transpiration rates are high (Flanagan et al., 1993; Wang et al., 1998). Moreover, night-time values can only be represented by the Péclet model when nonsteady-state conditions are also considered, a finding that is in good agreement with recent observations (Cernusak et al., 2005; Farquhar & Cernusak, 2005; Cuntz et al., 2007). The calculated scaled effective path length (L) for water movement from the veins to the site of evaporation for the four different species is well within the range reported in the literature (0.004–0.17 m from Wang et al., 1998; Table 3). Slight differences among values of L observed here and from literature data of the same or related species are expected as we should assume that L is not constant for a given species but affected by environmental conditions such as water relations (Ferrio et al., 2009, 2012), related to leaf development stage and age (Barnard et al., 2007), and dependent on transpiration rate (Song et al., 2013).
Table 3. The calculated effective path length L determined in this study compared to values of the same or of related species obtained from the literature
Species examined here
Same or related species from literature
Depending on water availability; lower values with optimum water supply, high values under drought conditions.
While the leaf water-soluble OM shows the expected 18O enrichment in all species examined, phloem sugars do not match predictions in some
When comparing mean daily Δ18OL (weighted for photosynthesis or photosynthetic active radiation) with leaf water-soluble OM (Table 2), the enrichment of organic oxygen above water is very close to the expected 27‰ for the three broadleaf species and slightly lower for pine and larch, but still within the range reported for recent assimilates in other species. In Ricinus communis, for example, the enrichment of recent assimilates above leaf water can vary between 25.4 and 27.1‰ (Barbour et al., 2000; Cernusak et al., 2003; Gessler et al., 2007b). Leaf water-soluble OM is a mixture of mainly sugars, organic acids and amino acids. Slight deviations in the oxygen isotope enrichment from the average 27‰ might be attributed to compounds containing not only carbonyl oxygen, but also oxygen in other functional groups, which might differ in their isotopic composition. Whereas Δ18O was comparable between leaf water-soluble and phloem OM in beech and oak, phloem OM was depleted by c. 2‰ in pine and by < 4‰ in Alpine ash and larch. As a consequence, 18O enrichment of phloem OM above water was clearly lower than the expected 27‰ (Table 2). Figure 3 indicates that leaf water isotopic enrichment was more variable during the diel course than was Δ18O in the phloem. The damped temporal variation of phloem OM points to a longer integration of the evaporative conditions imprinted in the oxygen isotope enrichment due to longer turnover times of this OM pool. Barnard et al. (2007) calculated approximate turnover times between 6 and 12 h for soluble OM in pine needles, whereas leaf water turned over in c. 1 h during the light period. Moreover, it has been shown for various species that leaf water can turn over and reach steady-state values within almost 35 min (Wang & Yakir, 1995). Due to the time needed for phloem loading and transport, the isotopic signal arrives in the twig phloem with some additional delay. Brandes et al. (2006) observed that the isotopic time lag between leaf water-soluble and twig phloem OM in Scots pine was < 1 d. Together, the longer turnover time and the time needed for transport might indicate one of two hypotheses (or both): (1) that evaporative conditions and thus leaf water enrichment of the preceding day(s) affect phloem Δ18O and (2) that not only OM assimilated during the day, but also OM originating from transitory starch remobilized during the night contribute to phloem-transported compounds. Both factors could be partially responsible for the lower-than-expected 18O enrichment of phloem OM above leaf water in the two conifers and E. delegatensis. However, we can rule out (1) for pine and Alpine ash because the Δ18O of phloem OM was also clearly less enriched than the expected 27‰ when compared with photosynthesis-weighted modelled Δ18OLs of the preceding 2 d. Hypothesis (2) is based on the following assumption: during starch hydrolysis c. 6 out of 11 oxygen atoms of the produced sucrose are exchanged with the normally less enriched leaf water during the night (Gessler et al., 2007b). In our study, however, the average night-time Δ18OL was comparable with photosynthesis-weighted daytime values in both pine and Alpine ash (cf. Fig. 3). As a consequence, the contribution of starch-derived organic compounds could not explain the lower-than-expected Δ18O values for phloem OM.
Differences in the chemical composition of phloem OM are most likely not the reason for the lower-than-expected oxygen isotope enrichment
One reason for the relative depletion of the conifer phloem might be related to the chemical composition of organic compounds transported, as it is known that different compound classes differ in their oxygen isotope composition (Schmidt et al., 2001) and in their ability to exchange organic oxygen with water. The comparison between the phloem metabolome (weighted for oxygen atoms) of beech, oak and pine revealed that the most abundant compound was sucrose in all species and that the monosaccharides glucose and fructose only played a minor role. Glucose and fructose both have a free carbonyl group and could exchange one oxygen atom per molecule with phloem water. If we assume full exchange of each carbonyl oxygen of the monosaccharides with nonenriched source water, then this would cause a 18O depletion of phloem OM by c. 0.5‰; a value too small to explain the lower-than-expected 18O enrichment of pine phloem OM. The most obvious difference between beech, on the one hand, and oak and pine, on the other, is the relatively high contribution of cyclitols to organic oxygen in the phloem of the two latter species. To our knowledge, there is no information published on the compound-specific oxygen isotope composition of cyclitols, even though it is known that alcohols can be slightly 18O depleted compared to carbohydrates (Schmidt et al., 2001). If we were to assume that only pinitol, which contributes 5.6% to the organic oxygen, was responsible for the deviation of phloem OM from the expected 27‰ enrichment in pine, this compound would need to have an unrealistic Δ18O value of −35.5‰ (i.e. (23.5‰ – 0.944 × 27‰)/0.056). Moreover, in that case only pinitol and neither the precursor myo-inisitol (Kindl et al., 1966) present in beech and oak nor the other cyclitol quercitol should be strongly depleted. As a consequence, we can rule out differences in the chemical composition as being responsible for the observed differences in the 18O enrichment of phloem OM between species – at least based on the comparison between pine, on the one hand, and beech and oak, on the other.
Phloem loading and transport as well as bark photosynthesis might explain the 18O enrichment patterns in the phloem
The clear and significant difference in Δ18O between leaf water-soluble and phloem OM in the two coniferous species and in E. delegatensis might be best explained by exchange of organic oxygen with water less enriched than leaf water associated with (1) phloem loading and/or (2) phloem transport together with a contribution of assimilates originating from bark photosynthesis to phloem OM.
In contrast to broadleaf species where phloem loading occurs via the companion cells to the phloem in the minor veins which are located in close vicinity to the mesophyll cells (Lalonde et al., 2003), the phloem in the needles of conifers is loaded in the central cylinder, isolated by an endodermis from the needle mesophyll. The symplastic pre-phloem pathway for assimilate transport from the mesophyll cells crosses the bundle sheath, the transfusion parenchyma as well as the Strasburger cells before the sieve elements are reached (Liesche et al., 2011). If we now hypothesize that oxygen atom exchange occurs before or during phloem loading, explaining the low 18O enrichment of phloem sugars in the two conifers, the following would be prerequisites: the endodermis with the Casparian strips prevents, at least partially, the back-diffusion of enriched mesophyll water to the perfusion tissue so that at least the region directly around the axial phloem is mainly influenced by nonenriched xylem water. During the transport through the cells of the perfusion parenchyma and/or the Strasburger cells considerable amounts of the transport sugar sucrose need to be converted to substances with a free carbonyl group in order to be able to exchange oxygen atoms with the nonenriched water. A calculation with several simplifications illustrates the order of magnitude of the effect on Δ18O of the OM loaded into the phloem: we take into account only sucrose transported to the perfusion tissue where we assume it to be broken down to fructose and glucose; alternatively hexoses might be transported from the mesophyll to the sieve tubes. Glucose and fructose can exchange 1 oxygen atom per molecule and we assume fast equilibration between the two molecules so that 2 oxygen atoms can be exchanged per hexose. If sucrose is synthesized from hexoses within the central cylinder and loaded into the phloem, up to 3 of 11 oxygen atoms could have exchanged. We now bravely assume that the water with which the organic oxygen is exchanged is not evaporatively enriched at all (i.e. equalling the source water). Then the sucrose molecule in the phloem in pine would have a Δ18O of 8/11 × (11.4‰ + 27‰) + 3/11 × 27‰ = 35.3‰ when all exchangeable oxygen atoms had actually exchanged. (The photosynthesis-weighted Δ18OL in pine is 11.4‰ and 27‰ is the expected enrichment of carbonyl groups above water.) This calculated value is comparable with the measured Δ18O of bulk phloem OM of 35.1‰. The same calculation for larch results in values between 34.0‰ (measured 31.7‰) and 38.9‰ (measured 33.4‰). Our calculation shows that such a mechanism could in principle explain the Δ18O values in the pine but not in the larch phloem. It is, however, unlikely that the water for exchange in the needle central cylinder is only influenced by xylem and not by the 18O-enriched leaf water. If the needle endodermis were such an effective barrier against back diffusion of mesophyll water, causing the whole central portion of the needle water to be fully xylem-like, this would also affect our calculation of lamina needle water 18O enrichment (Eqn 2) computed from measured bulk needle water. If φx were increased and thus φL decreased, the calculated lamina mesophyll water enrichment would increase. An increase of φx to 20% would cause calculated photosynthesis-weighted Δ18OL in pine to increase by 2.5‰ and thus the Δ18O of phloem sucrose – as calculated above assuming the exchange of 3/11 oxygen atoms – would be 37.1‰; that is, clearly above the observed value.
In conclusion such oxygen atom exchanges processes could contribute to the observed decrease in Δ18O from leaf sugars to phloem OM in the two conifers to some extent but most likely cannot fully explain their lower than expected relative enrichment of OM in the phloem. Moreover the mechanism depicted above does not explain our observations in Alpine ash.
Offermann et al. (2011) proposed that the widely accepted theory of phloem transport (as recently reviewed by Van Bel, 2003) can offer an explanation for exchange of organic oxygen atoms with stem water. According to theory, phloem transport is associated with continuous unloading and reloading of sugars along the transport path. It has been shown that up to 6% of the phloem sugars are unloaded per cm of transport path and that two-thirds of these carbohydrates are reloaded into the sieve tubes again (Minchin & Thorpe, 1987). If we assume that part of the retrieved sugars underwent metabolic conversion in the parenchymatic tissues of the twig or trunk forming intermediates with exchangeable carbonyl groups, we could then explain the 18O depletion of phloem OM compared to leaf sugars. Moreover, bark photosynthesis and phloem loading of bark assimilated sugars could contribute to the lower-than-expected 18O enrichment in the phloem. Organic matter fixed (or refixed from respired CO2) in the bark, where reaction water is not or only slightly enriched, should have a Δ18O value of c. 27‰ above source water (Cernusak et al., 2005), well below the enrichment for sugars fixed in leaves and the values observed in phloem OM of the two conifers and Alpine ash. Thus bark photosynthesis, which mainly occurs in young twigs, could contribute to the twig phloem OM of pine, larch and ash trees and explain the observed Δ18O values. In fact, Berveiller et al. (2007) observed higher maximum gross photosynthetic rates under light-saturated conditions for stem photosynthesis for pine (2.9 μmol m−2 s−1) than for beech and oak. There is no information on the photosynthetic capacity of the bark of E. delegatensis, but Tausz et al. (2005) found that the sun-exposed bark of Eucalyptus nitens has the photochemical properties and the pigment composition of a sun leaf. Tausz et al. (2005) conclude that twig and stem CO2 fixation is thus likely to be important in smooth-barked eucalypts (such as E. delegatensis), because the leaf area index of eucalypt forests is low compared to European beech or oak forests, and eucalypt leaves are pendulous. The same is true for the two conifers examined, which have very sparse canopies and low LAI (Brandes et al., 2007) and thus self-shading of the bark by leaves is lower than for the two broadleaf species. As a consequence, it is probable that actual bark photosynthesis is higher in the two conifers and in Alpine ash than in beech and oak, thus contributing to an explanation for the observed lower oxygen enrichment in the phloem-transported sugars.
In conclusion, we demonstrate here that even though leaf water enrichment seems to be imprinted on leaf assimilates as expected, the phloem-transported OM enrichment strongly differs between the two deciduous broadleaf species, on the one hand, and the two conifers and the evergreen broadleaf species, on the other. We have presented two mechanisms related to (1) phloem loading in the conifers and to (2) phloem transport and bark photosynthesis, that could explain the lower-than-expected evaporative enrichment of phloem OM in three out of five species examined. Both mechanisms cause a decoupling of the original leaf-level isotope signal, thus affecting the interpretation of the oxygen isotopic signature in heterotrophic tissues including tree rings. The findings in our study point to the possibility that oxygen atom exchange with xylem water might occur not only during cellulose synthesis in the stem, but also – at least in some species – before the sugars arrive in the cambial tissues. In the conifers and the eucalypt species the ‘oxygen atom exchange’ (assuming the exchanged water equals source water) calculated for phloem sugars ranges between 30% (pine) and 63% (larch treeline). It should be noted that the values we calculate here are not necessarily exchange sensu strictu, but also include mixing of sugars produced in a nonenriched aqueous environment. Nevertheless, the values describe the decoupling between leaf water enrichment and the Δ18O of OM. The values are comparable to or even higher than the average exchange of 42% assumed for cellulose synthesis from sucrose (Cernusak et al., 2005), and need to be taken into account when studying tree ring δ18O. Figure 4(c) (pine) might imply that the phloem OM values only show an offset compared to leaf assimilates, but the results from larch (Fig. 4e) suggest that the difference might not be constant, and may depend on environmental conditions and phenology. Our results demonstrate that we need to obtain more information about the mechanisms that control the transfer of the oxygen isotopic signal from the leaf to heterotrophic tissues. This is of particular importance for tree ring-based climate reconstructions and for studies that explore the oxygen isotope signature of the tree ring archive to study plant–climate interactions. Without knowledge of the mechanisms that uncouple the cellulose oxygen isotope signal from leaf level signals and the quantitative extent of this uncoupling, the interpretation of the tree ring oxygen isotope composition will remain error-prone.
A.G. acknowledges support by the Deutsche Forschungsgemeinschaft (DFG) under contract numbers GE 1090/8-1 and 9-1. Meteorological data for the Hartheim and Tumbarumba site were provided by Helmut Mayer and Ray Leuning, respectively. G.D.F. acknowledges support from the Australian Research Council through DP110105376. Data development in the Lötschental was supported by the Swiss National Science Foundation (200021_130112 ‘ISOPATH' 200021_121859 ‘INTEGRAL’). We thank Matthias Saurer for carrying out part of the leaf water extraction.