INTRODUCTION

TOP ABSTRACT INTRODUCTION RESULTS AND DISCUSSION MATERIALS AND METHODS LITERATURE CITED

Natural variation in ¹⁸O content (¹⁸O) of CO₂ is a useful tracer for photosynthetic activity. This is due to a sequence of events: first, ¹⁸O of chloroplast water is high due to evaporative effects (Gonfiantini et al., 1965); second, in the chloroplasts, exchange of oxygen between CO₂ and H₂O is catalyzed by carbonic anhydrase (CA); and third, a large fraction of this ¹⁸O-labeled CO₂ diffuses from the chloroplast back to the atmosphere. On a leaf scale, this "retroflux" of ¹⁸O-enriched CO₂ from the leaf back to the atmosphere is observed as an enrichment in the C¹⁸OO in air passing over the leaf or as discrimination against C¹⁸OO by the leaf (¹⁸O) (Farquhar and Lloyd, 1993). Notably, ¹⁸O is also observed on a global scale as latitudinal and seasonal changes in the ¹⁸O of atmospheric CO₂. The quantitative use of such large-scale signals, however, still critically depends on better understanding of the basic processes influencing ¹⁸O (Francey and Tans, 1987; Farquhar et al., 1993; Ciais et al., 1997).

To interpret ¹⁸O measured during leaf-atmosphere CO₂ exchange, an estimate of CO₂ concentration at the site of CO₂-H₂O is required (Farquhar and Lloyd, 1993). The chloroplast CO₂ concentration (c_c) may be derived from comparing measured and modeled discrimination against ¹³CO₂ (¹³C) (Farquhar et al., 1982; Evans et al., 1986; von Caemmerer and Evans, 1991). Since both the photosynthetic enzyme Rubisco (responsible for ¹³C discrimination) and CA (responsible for ¹⁸O) are similarly distributed within the chloroplast stroma (Anderson et al., 1996), the ¹³C-derived value of c_c was also applied to ¹⁸O (Farquhar et al., 1993; Flanagan et al., 1994). However, it was suggested (Yakir, 1998) that the CO₂ concentration pertaining to ¹⁸O may be associated with the chloroplast surface, i.e. the limit of CA activity, and not the mean CO₂ concentration at sites of CO₂ fixation by Rubisco. This is because CA acts to cancel out any gradients in ¹⁸O of CO₂ within its domain. We now suggest that with adequate estimates of chloroplast water ¹⁸O and of the extent of CO₂-H₂O isotopic equilibrium in the chloroplast (i.e. CA activity), it should be possible to use ¹⁸O to accurately estimate the effective CO₂ concentration at the sites of CO₂-H₂O equilibrium. This approach is somewhat similar to that using observed and predicted ¹³C to compare c_i and c_c (von Caemmerer and Evans, 1991).

Using ¹³C-derived estimates of c_c, the internal leaf conductance to CO₂ (g_i) and its influence on leaf photosynthesis have been well characterized (von Caemmerer and Evans, 1991; Lloyd et al., 1992; Loreto et al., 1992; Syvertsen et al., 1995). However, evaluating the relative importance of the major components of g_i, the wall conductance (g_w) and the chloroplast conductance (g_ch) has been restricted (Cowan, 1986; Evans et al., 1994). The association of ¹⁸O with CO₂ concentration at the chloroplast surface should enable this partitioning. Information on CA activity directly from assays or through ¹⁸O measurements should also provide insight into the role of CA in facilitating diffusion within the chloroplast (Cowan, 1986; Makino et al., 1992; Price et al., 1994; Williams et al., 1996).

By comparing the CO₂ concentration and isotopic composition of air entering and leaving a leaf chamber, dis-crimination against C¹⁸OO (¹⁸O) may be measured "on-line" in a method equivalent to ¹³C (Evans et al., 1986):

(1)

where  = c_in/(c_in-c_o), c_in, c_o, and _in, _o referring to the CO₂ concentration (corrected to the same humidity) and isotopic composition of air entering and leaving the cuvette, respectively. ¹⁸O can also be predicted (Farquhar and Lloyd, 1993) as

(2)

where _ea = 1,000·[(_e/1,000 +1)/(_a/1,000 + 1) 1];  = c_c/(c_a  c_c); _a and _e represent the ¹⁸O of CO₂ in the overlying air and in full isotopic equilibrium with water in the chloroplast, respectively, and c_a and c_c the respective CO₂ concentrations (see Fig. 1); is the weighted-mean diffusional fractionation through the boundary layer, 5.8, stomata, 8.8, and aqueous leaf media, 0.8, (Farquhar and Lloyd, 1993). Despite general agreement between modeled and measured ¹⁸O (Farquhar et al., 1993; Flanagan et al., 1994; Williams et al., 1996), large quantitative discrepancies often occur (Yakir et al., 1994; Williams et al., 1996; Harwood et al., 1998; Wang et al., 1998). There are three main assumptions in Equation 2: (a) chloroplast water (and hence CO₂ in equilibrium with this water) is assumed to be isotopically similar to water at the evaporating sites (_e); (b) CO₂ and H₂O in the chloroplast reach full isotopic equilibrium; and (c) c_c correctly represents the CO₂ concentration at the site of oxygen exchange.

View larger version (38K): [in this window] [in a new window]   Figure 1.   Diagram showing the 18O content in fluxes of CO2 (Fout) and H2O (E) from leaf to atmosphere. H2O enters the leaf with isotopic composition s, evaporates from the cell surfaces, and diffuses from the leaf, experiencing both phase-change (*) and diffusional (k) fractionation, giving rise to depleted transpiring water (t) and enriched evaporating surfaces (e). Similarly, CO2 from the atmosphere (Fin) dissolves in the chloroplast, equilibrates (eq) to composition c depending on the 18O of water in the chloroplast and the extent of isotopic equilibrium (eq), and then approximately two-thirds retro-diffuses outward (Fout) with fractionation during diffusion (). This can be observed as an 18O enrichment in outgoing CO2 (out) relative to incoming CO2 (in), which is proportional to discrimination against C18OO, termed 18O. CO2 reference points along the leaf-atmosphere pathway are marked (with average values in µmol mol1) as cc, ccs, ci, and ca, referring to the CO2 concentration in the chloroplast, chloroplast surface, substomatal cavity, and air, respectively.

The isotopic composition of water at evaporating surfaces (_e) may be estimated from the Craig and Gordon model of evaporative enrichment (Craig and Gordon, 1965):

(3)

where h* is the relative humidity at leaf temperature; _a and _t are the isotopic composition of water vapor in the air and transpired by the leaf, respectively; _k is the combined diffusional fractionation through stomata and turbulent boundary layer (Farquhar and Lloyd, 1993; Buhay et al., 1996); and * is the temperature-dependent liquid-vapor fractionation. The measurement of ¹⁸O of transpired water vapor (_t) allows estimation of _e under non-steady-state conditions (Harwood et al., 1998). While the proximity of chloroplasts to the liquid-air interface in leaves implies good mixing between evaporating sites and chloroplasts, isotopic gradients in leaf water can occur (Yakir et al., 1989, 1994; Luo and Sternberg, 1992; Wang and Yakir, 1995) and need to be considered.

Considering oxygen isotope exchange between CO₂-H₂O, current estimates have suggested isotopic exchange to be almost complete, approximately 95% (Farquhar and Lloyd, 1993; Flanagan et al., 1994; Williams et al., 1996). However, given the potential uncertainties in ¹⁸O of water and CO₂ concentration in the chloroplast when interpreting ¹⁸O, an independent method is still required to test this assumption. Alternatively, the extent of isotopic equilibrium (_eq) in the CO₂-H₂O system may be derived from Mills and Urey (1940) as:

(4)

which describes the fractional approach to full equilibrium (where _eq = 1) as a function of the number of hydration reactions achieved per CO₂ molecule (k). This "coefficient of CO₂ hydration" may be calculated for a leaf by calculating the rate constant (k) from biochemical measurements of CA activity and the residence time of CO₂ in the leaf () from photosynthetic flux measurements of CO₂ (see "Materials and Methods"). In this way, the extent of isotopic equilibrium may be directly determined.

We sought to determine the CO₂ concentration relevant to CO₂-H₂O in leaves from measurements of ¹⁸O by constraining both the ¹⁸O of exchangeable water and the extent of isotopic equilibrium as above. The subsequent implications toward internal CO₂ conductance are discussed in the context of CA activity and its role in facilitating diffusion of CO₂ within the chloroplast.

	RESULTS AND DISCUSSION

TOP ABSTRACT INTRODUCTION RESULTS AND DISCUSSION MATERIALS AND METHODS LITERATURE CITED

Interpreting C¹⁸OO discrimination requires information on ¹⁸O of water in the chloroplasts, the extent of isotopic equilibrium between CO₂-H₂O and the CO₂ concentration in the chloroplast. The ¹⁸O value of chloroplast water is often derived from the Craig and Gordon model for evaporating water (_e in Eq. 3; Flanagan et al., 1994; Williams et al., 1996; Yakir and Wang, 1996; Wang et al., 1998; Harwood et al., 1998). This is due to the proximity of chloroplasts to the liquid-air interfaces within leaves. This leaves two options in using Equation 2 and measurements of ¹⁸O: (a) to use ¹³C-derived estimates of c_c as the CO₂ concentration relevant to the site of oxygen exchange in the chloroplast and solve for the extent of isotopic equilibrium (e.g. Flanagan et al., 1994); and (b) to independently measure the extent of isotopic equilibrium and solve for c_c. We argue that c_c does not refer to the site of CO₂-H₂O equilibrium and so took the latter approach to estimate its true value. Using constrained estimates of _e and direct assays of CA activity, we solved both ¹⁸O and ¹³C discrimination equations for c_c. We found the ¹⁸O-derived c_c to be always higher than ¹³C-derived values, and define the CO₂ concentration relevant to ¹⁸O as c_cs (for [CO₂] at the chloroplast surface). We then use c_cs to partition the internal conductance into its two major components. In the following sections we show how the interpretations were constrained and discuss their implications.

Observed ¹⁸O

Consistent with previous observations and predictions, a clear dependence of ¹⁸O on c_c/c_a was observed (Fig. 2; Farquhar et al., 1993; Flanagan et al., 1994; Williams and Flanagan, 1996; Williams et al., 1996). As expected, ¹⁸O was also larger when measured using ¹⁸O-depleted source CO₂, which generated a larger isotopic difference between source and leaf CO₂ (_ca) (increasing the precision of measurement). No difference in the response was observed under different photorespiratory conditions in oak leaves (Fig. 2c). Low pO₂ did, however, induce higher assimilation rates and lower c_i and c_c (Table I) due to reduced photorespiration. Estimates of internal CO₂ conductance (g_i) derived from ¹³C measurements were 0.50 (±0.12), 0.32 (±0.05), and 0.27 (±0.09) mol m² s¹ for tobacco, soy, and oak respectively, which were used to calculate c_c/c_a. Our g_i estimates were in line with previous estimates on similar herbaceous species (von Caemmerer and Evans, 1991; Evans et al., 1994), although in the case of oak, g_i was higher than the range previously quoted for oak species (0.15, Loreto et al., 1992; 0.08-0.22 mol m² s¹, Roupsard et al., 1996; 0.07-0.08, Hanba et al., 1999).

View larger version (10K): [in this window] [in a new window]   Figure 2.   Discrimination against C18OO (18O) as a function of chloroplast CO2 concentration (calculated from 13C) and expressed as cc/ca for tobacco (a), soy (b), and oak (c). In a and b, experiments were conducted under depleted source CO2 (30, white symbols) and ambient CO2 (0, black symbols). For oak, experiments were conducted all in depleted CO2, but at 2% (squares), 21% (circles), and 35% (triangles) oxygen.

View this table: [in this window] [in a new window]   Table I.   Gas exchange (at max PPFD), CA activity, and isotopic water data (average at all PPFDs) for tobacco, soy (n = 3 and 2), and oak (n = 3, at different O2%) Units are: evaporation rate (Emax, mmol m2 s1), stomatal CO2 conductance (gs(max), mmol CO2 m2 s1), CO2 assimilation (Amax, µmol m2 s1), sub-stomatal CO2 concentration (ci, µmol mol1), leaf temperature (Tmax, °C), carbonic anhydrase CO2 hydration rate, under assay (CAassay, at 2°C and 35 mM [CO2], mean of three leaves), and in vivo conditions (CAleaf, at ccs and Tleaf, µmol CO2 m2 s1). For VPD (kPa) and isotopic data (), nos. are averages (+SD) during the entire light response. Symbols as in text.

¹⁸O of Water at the Site of Oxygen Exchange

Estimates of evaporating surface water (_e) were based on direct measurements of transpired water vapor (_t) applying the isotopic fractionation during evaporation (Eq. 3). The maintenance of constant vapor pressure deficit (VPD) during the complete photosynthetic photon flux density (PPFD) curve kept both _t and _e constant throughout each experiment (Table I). Determining _e in this way from _t avoids uncertainties that arise in substituting source water ¹⁸O for _t in Equation 3, as shown in Table I; although _t is at steady state, the absolute value may differ from source water (4.5) by several per mill.

_e is assumed to provide a close approximation to ¹⁸O of water in the chloroplasts. The proximity of chloroplasts to evaporating surfaces is sufficient to ensure good isotopic mixing between the two. In particular, this assumption would be safe when ¹⁸O heterogeneity in the entire leaf water is small. As a precautionary measure, such heterogeneity was evaluated by comparing _e with measured bulk leaf water (_LW) both at the end of each light response experiment (Table I; Fig. 3, white symbols) and across a range of evaporation rates in an independent test (Fig. 3, black symbols). On average, bulk leaf water was lower than _e by 2 (±1 in Fig. 3). This phenomenon has been observed extensively (Wang et al., 1998, and refs. therein) and has been partly explained by the inclusion of unenriched vein water, estimated to represent 2% to 5% of total leaf water (Yakir et al., 1989; Flanagan et al., 1991), and/or by a Peclet effect proposed by Farquhar and Lloyd (1993).

View larger version (16K): [in this window] [in a new window]   Figure 3.   The difference between e from the Craig and Gordon equation and bulk leaf water (LW) as a function of evaporation rate (E) for soy (triangles), tobacco (circles), maize (diamonds), and sorghum (squares). White symbols are data from the last measurement of the light response study; black symbols are additional points from the leaf water heterogeneity test. The three marked points excluded from statistical analysis are thought to represent non-steady-state conditions.

The difference between _e and _LW increased with the evaporation rate (Fig. 3, excluding the three marked data points, from leaves thought not to be at isotopic steady state), which is consistent with a Peclet effect (Flanagan et al., 1991; Farqhuar and Lloyd, 1993). In this case, the large advective flux of water through the leaf at higher evaporation rates restricts back-mixing of ¹⁸O-enriched water from the evaporation sites with the bulk leaf water. The maximal Peclet effect observed here was 3 (excluding marked points), which was much smaller than those reported previously (Flanagan et al., 1991, 1994; Wang et al., 1998). The small Peclet effect in this study was probably due to low evaporation rates (<5 mmol H₂O m² s¹, Table I). In addition, although not measured here, Peclet effects in oak (K.G. Harwood, D. Yakir, J.S. Gillon, and H. Griffiths, unpublished data) and other woody species (birch and poplar; Roden and Ehleringer, 1999) have been consistently equally low in a wide range of conditions. Therefore, the absence of significant isotopic gradients in leaf water over the whole leaf is a good indication that isotopic gradients are unlikely to occur across the much smaller distances (<0.01 mm) between evaporating surfaces and chloroplasts.

Extent of CO₂-H₂O Isotopic Equilibrium

We measured CA activity in the experimental plants and used the results to estimate the in vivo extent of isotopic equilibrium between CO₂ and H₂O in the chloroplast. Previously, close to full isotopic equilibrium has been assumed due to the high rates of CA catalysis expected in most plants. We tested this assumption by measuring CA activities under assay conditions and estimating in vivo rates under leaf conditions (at chloroplastic [CO₂] and leaf temperature). Assay rates showed significant variation, with the lowest rates in soy (Table I). Although CA activity for the oak plants used here was not determined, measurements in oak species from previous studies revealed very high CA activity (mean and SD for Quercus bosserii 288 ± 36; Quercus robur 261 ± 25; Quercus pedunculata 201 ± 30 mmol CO₂ m² s¹; J.S. Gillon and D. Yakir, unpublished survey data). Further differences were introduced when calculating in vivo CO₂ hydration rates, due to small variabilities in leaf temperature and internal [CO₂] between the experiments. Notably, during a light response curve, CO₂ hydration rates in vivo did not vary considerably. Most likely, reductions in the calculated CO₂ hydration rate associated with decreased internal [CO₂] at high light were compensated for by increased leaf temperatures and enhancement of catalytic activity.

Using the data on CA activity during leaf gas exchange, we could assess the extent of CO₂-H₂O isotopic equilibrium independently of ¹⁸O measurements. The efficiency of CO₂-H₂O isotopic equilibrium depends upon the product k, which is residence time () times the rate constant of CO₂ hydration within the chloroplast (k) (see "Materials and Methods"). Combining with the isotope exchange theory of Mills and Urey (1940) for the CO₂-H₂O reaction, the fractional extent of isotopic equilibrium may be described by _eq (Eq. 4), so that full equilibrium occurs when _eq = 1 (corresponding to k greater than 15; Fig. 4). Thus, as CO₂ (with isotopic signal of _a) passes through a leaf, the ¹⁸O of CO₂ changes, approaching equilibrium with leaf water represented by _e. The ¹⁸O value of CO₂ in the chloroplast (_c) should lie between _a and _e, at some point depending on _eq (Fig. 4). This effect has already been demonstrated qualitatively in genetically modified plants with low CA activity, where ¹⁸O, and therefore _c, were dramatically reduced compared with the values expected at full isotopic equilibrium (_e) (Price et al., 1994; Williams et al., 1996).

View larger version (18K): [in this window] [in a new window]   Figure 4.   Diagram showing the dynamics of oxygen isotope exchange between atmospheric CO2 (a) and leaf water (e) and the resulting 18O of CO2 (c). Isotopic equilibrium (eq) from Equation 4, solid line was calculated from the CA activity and CO2 residence time (k), which represents the number of hydrations per CO2 molecule and is related to ca/ea.

Calculating k and the corresponding extent of isotopic equilibrium for each data point, we observed more than 95% isotopic equilibrium (_eq >0.95) for tobacco (Fig. 5). The lower CA activity in soy suggested that the equilibrium was 75% complete. In the extreme case, potentially high CA activity in oak corresponded to complete isotopic equilibrium throughout the light response, where k was always greater than 15 (data not plotted in Fig. 5). Note that in other plants, including C3 and C4 species, _eq values were found to span the whole range from 0 to 1 (J.S. Gillon and D. Yakir, unpublished data).

View larger version (24K): [in this window] [in a new window]   Figure 5.   The number of hydration reactions per CO2 molecule (k) calculated from CAleaf/Fin as a function of the CO2 assimilation rate. Shown on the second axis is the equivalent extent of isotopic equilibrium from Equation 4, in which full equilibrium (>99.5%) occurs above k = 15. White symbols, Soy; black symbols, tobacco (different symbols refer to different light responses). All values for oak were above k = 15 because of the assumed high CA rates.

CO₂ Concentration at the Site of Isotopic Equilibrium

Based on the above discussion that _c lies between _a and _e and reflects _eq, it is possible to show that _eq is related to _ca/_ea (Fig. 4), since algebraically:

(5)

This describes the ¹⁸O/¹⁶O ratio of CO₂ at the site of oxygen exchange (R_c) relative to that in full equilibrium with leaf water (R_e), and that for un-equilibrated CO₂ inside the leaf, R_c'. The term R_c' = R_{a · (1/[+1]) allows for the variable expression of under non-equilibrium conditions (as in ¹³}C discrimination). Thus, (1e^k/3) = _eq  ca/_ea (Fig 5). We now incorporate the extent of isotopic equilibrium into Eq. 2, and C¹⁸OO discrimination is then given as:

(6)

With measured values of ¹⁸O, _ea, and _eq, we may thus derive , and hence c_c(eff), the effective CO₂ concentration at the site of CO₂-H₂O equilibrium.

The c_c(eff) values obtained from Equation 6 were always intermediate between c_i (from gas exchange) and c_c (from ¹³C), as shown in Figure 6. These results were obtained from eight experiments in three species, measured on two separate systems, reducing the likelihood of bias introduced via system or species effects. Typically, all values of internal [CO₂] dropped at high assimilation rates, as CO₂ demand increased, albeit with variation due to some non-correlated changes in stomatal conductance, particularly for soy. Species differences were evident: c_c(eff) was generally closer to c_i in soy, closer to c_c in oak, and intermediate in tobacco.

View larger version (31K): [in this window] [in a new window]   Figure 6.   Data shown for all light response curves, showing internal CO2 concentration (µmol mol1) as a function of CO2 assimilation rate (A) (µmol m2 s1). Symbols refer to CO2 concentration in internal air space (ci) (from gas exchange measurements, ), ccs (from 18O, e, and CA activity; ), and cc (from 13C; ). Species are tobacco (a-c), soy (d-e), and oak (f-h). Light responses in c and e were conducted using ambient 18O CO2, whereas the rest used CO2 depleted in 18O. f through h, Experiments in 40%, 20%, and 2% ) O2, respectively.

The values of c_c(eff) represent the CO₂ concentration at the effective site of CO₂-H₂O equilibrium, which we term c_cs (Yakir, 1998), indicating that the chloroplast surface is the likely site. This assumes that the limit of CA activity occurs at the chloroplast surface, since the majority of CA resides within the chloroplast (Everson, 1970). These results are consistent with the difference between the effects of Rubisco on ¹³C and CA on ¹⁸O: although Rubisco and CA show the same distribution within the chloroplast (Anderson et al., 1996), Rubisco removes ¹²CO₂ from the system, creating a ¹³C gradient between c_c and c_a; CA only acts to cancel out any ¹⁸O gradients in CO₂ throughout the domain of its activity, so that an ¹⁸O gradient only exists from the chloroplast surface (c_cs) to the atmosphere (c_a) (Fig. 7).

View larger version (19K): [in this window] [in a new window]   Figure 7.   Diagram representing the backflux of CO2 from sites of CO2 fixation (cc) and sites of oxygen exchange (ccs) in the chloroplast, showing the partitioning of total internal conductance (gi) (relevant to 13C) into chloroplast (gch) and wall (gw) conductance (from 18O).

Note that in interpreting ¹⁸O, the best-constrained value is _e. Consequently, testing the model for ¹⁸O usually involved deriving _c values and comparing them with _e values. Assuming that we appropriately adjust _c for _eq and correctly estimate c_cs, the two values should match. In previous studies, ¹³C-derived values of c_c were used and the observed difference between _e and _c was explained in terms of incomplete isotopic equilibrium. The effects of incomplete equilibrium was addressed in those cases by applying a certain  value ( = A/CA_leaf), which was incorporated within the ¹⁸O model (Farquhar and Lloyd, 1993; Flanagan et al., 1994; Williams and Flanagan, 1996; Williams et al., 1996). Furthermore, the method of c_c determination based on individual ¹³C measurements (and not the trend of ¹³C across the full range of A) generated a range of c_c values (up to 40 µmol mol¹), so that co-adjustment of c_c and  was required to resolve _e versus _c differences.

In some cases, estimates of _c were as much as 10 below _e in both laboratory and field studies (Yakir et al., 1994; Harwood et al., 1998; Wang et al., 1998). Such differences cannot be explained by only considering c_cs, and probably imply large heterogeneity in leaf water isotopic composition. Especially in the two latter field studies, Peclet effects may be much larger than observed in this study. It is possible that these discrepancies represent isotopic leaf water heterogeneity between water in the chloroplast and at the evaporating sites. Better characterization of the oxygen exchange site may help future studies of significant leaf water gradients and Peclet effects.

Partitioning Internal CO₂ Conductance

The association of ¹⁸O with the [CO₂] at the chloroplast surface (c_cs) provides us with another reference point in the diffusion pathway from atmosphere to chloroplast in addition to probing c_i via gas exchange (von Caemmerer and Farquhar, 1981) and c_c from ¹³C analysis (von Caemmerer and Evans, 1991). From Fick's law of diffusion, CO₂ concentration gradients are related to conductance by the general expression A = g_x (c₁  c₂). Applying values of c_cs, we may partition the total conductance (g_i) into its components before and after the chloroplast surface by plotting A versus (c_i  c_cs) and versus (c_cs  c_c). In each case, the inverse of the gradient refers to cell wall/plasmalemma conductance (g_w) and conductance within the chloroplast (g_ch), respectively (Fig. 7), assuming no significant resistance to CO₂ diffusion in the gaseous leaf interior (Evans et al., 1994). Despite a larger error in determining conductances from ¹⁸O compared with ¹³C, g_w was significantly higher than g_i for both tobacco and soy, and on the borderline of significance for oak (Table II). Comparing the values of g_ch relative to g_w, the chloroplast conductance was estimated to be 0.8 (tobacco), 0.3 (soy), and 3.2 (oak) times the wall conductance (g_ch/g_w, Table II). The magnitude and species variability of g_ch was much lower than previous theoretical estimations, where the wall conductance was thought to be the major limitation to diffusion, such that g_ch/g_w was predicted to be from 4.8 (Evans et al., 1994) to 7.4 (Cowan, 1986). The occurrence of low chloroplast conductance was associated with low in vivo CA activities (soy), while potentially high CA activity in oak may be associated with high g_ch.

View this table: [in this window] [in a new window]   Table II.   The breakdown of total leaf CO2 conductance (gleaf) into its components, stomatal (gs) (from gas exchange) and internal (gi) (from 13C, plus error from 95% confidence limits of the slopes) With 18O, gi is further partitioned into wall conductance to Ccs, gw, and the residual conductance within the chloroplast, (gch). All units are mol CO2 m2 s1. The ratio of chloroplast to wall conductance is also shown gch/gw. Average CAleaf activity is shown for comparison (µmol m2 s1).

Importance of CA-Mediated Diffusion in g_ch

It is becoming increasingly evident that CA facilitates diffusion and therefore CO₂ conductance within the chloroplast (Cowan, 1986; Makino et al., 1992; Price et al., 1994; Williams et al., 1996; Sasaki et al., 1998). This may be further supported by the association of CA activity with the relative magnitude of chloroplast conductance in the three species used here (Table II). However, in the past, modification of CA activity has revealed little or no change in photosynthetic rate (Price et al., 1994; Williams et al., 1996), so that the benefit to photosynthesis from CA remains unclear. We now propose that the relative contribution from CA to photosynthetic efficiency may be species dependent and not always clearly apparent. In particular, CA-mediated diffusion may be more important when total internal conductance is low, as is the case for woody species (von Caemmerer and Evans, 1991; Lloyd et al., 1992; Loreto et al., 1992; Syvertsen et al., 1995). In such cases, photosynthetic limitations attributable to low wall conductance (g_w), which occur due to the cellular architecture of schlerophyllous leaves, may be offset by optimizing chloroplast conductance (g_ch).

This species effect on CA-mediated g_ch is illustrated by estimating CO₂ assimilation as a function of chloroplast conductance (Fig. 8). Assimilation was described as A = k(c_c  *)  R_d, where k and * are the carboxylation efficiency and compensation point (k = 0.121 and 0.073, c_i = 208 and 252, * = 40 and 45 for oak and tobacco, respectively) and c_c = c_i  A/g_i. We calculated the change in CO₂ assimilation rate relative to observed values (Fig. 8) due to varying the chloroplast component of internal conductance (while keeping g_w constant, plotted as g_ch/g_w in Fig. 8). In oak, with lower wall conductance (high g_ch/g_w), the current assimilation rate is 20% higher compared with that which would occur at chloroplast conductance values found in tobacco. Conversely, in tobacco, increasing g_ch to the extent found in oak would result in only a 5% increase in A. This example is also consistent with the gas exchange measurements from tobacco plants with genetically reduced CA activity (Price et al., 1994; Williams et al., 1996). Internal conductance was lower (approximately 0.25 mol m² s¹) in the CA mutant compared with wild-type plants (approximately 0.4 mol m² s¹).

View larger version (23K): [in this window] [in a new window]   Figure 8.   The potential change in CO2 assimilation rate (A) as a function of gch (oak and tobacco, solid lines). gch is normalized relative to a constant wall conductance (gw) (0.35 and 1.12 mol m2 s1 for oak and tobacco, respectively). The changes in A are expressed relative to measured assimilation rates at actual conductance values, gch/gw = 0.8 and 3.2 for tobacco (A = 12.7 µmol mol1) and oak (A = 13.7 µmol mol1), respectively. Also marked is the estimated gch/gw (see text) of tobacco mutants lacking CA (Price et al., 1994; Williams et al., 1996), indicating only a small effect on assimilation relative to the wild-type tobacco.

Applying the present ratio of g_ch/g_w (0.8) for wild-type tobacco plants, we may calculate the wall conductance for wild-type plants from their ¹³C-derived g_i values. Assuming this physical wall conductance is unchanged between wild-type and CA mutant plants (the antisense CA gene should have no other effects on leaf physiology and structure), we estimate a lower value of g_ch/g_w = 0.5 for the CA mutant tobacco plants, i.e. the reduction in g_i is due to reduction in g_ch only. Indicating the position of the CA-mutant plants on Figure 8, we predict only a 5% drop in CO₂ assimilation for the 90% to 95% reduction in CA activity, in agreement with reported results.

Two main points arise from this simple analysis. First, it appears that relative chloroplast conductance is proportional to CA activity across almost three orders of magnitude of CA activity, with a possible minimum at g_ch/g_w = 0.5, where all residual CO₂ diffusion will be un-facilitated (i.e. no CA effect). This strongly supports the occurrence of CA-mediated diffusion in the chloroplast. Second, although the oak plants used may not be completely representative of woody species, CA activity in woody plants in general may have been optimized over evolutionary time to compensate for low wall conductance (J.S. Gillon and D. Yakir, unpublished data). For example, in a preliminary survey, mean in vivo CA hydration rates were 1,090 and 390 µmol m² s¹ for trees/shrubs (n = 16) and herbaceous species (n = 12), respectively, which may correspond to a three-times increase in g_ch relative to g_w. By extending such surveys to include conductance estimates (both internal and stomatal), or by manipulating CA activity in species with low internal conductance, the potential importance of CA in photosynthesis may prove to be substantially greater than currently assumed.

	MATERIALS AND METHODS

TOP ABSTRACT INTRODUCTION RESULTS AND DISCUSSION MATERIALS AND METHODS LITERATURE CITED

Plant Material

Soy (Glycine max), tobacco (Nicotiana tabacum), maize (Zea mays), and sorghum (Sorghum bicolor) were grown from seed in a greenhouse under ambient light and temperature at Weizmann Institute of Science (WIS). The latter two species were only used in the test of leaf water heterogeneity to increase the scope of the test. Oak seedlings (Quercus robur) were provided by the Forestry Commission (UK) in 1991, and kept outside and well-watered in 1-L pots at Moorbank Botanical Gardens (University of Newcastle-upon-Tyne, UK), until required. Measurements were conducted on 6- to 10-week-old plants of soy and tobacco plants and on 5-year-old oak seedlings. Transfer of plant material was several days prior to the experiment to allow acclimatization to laboratory conditions.

System 1 (WIS): Gas Exchange

Figure 9 shows a scheme of the on-line isotope/gas exchange system at WIS. Synthetic air was mixed from N₂, CO₂, and O₂ cylinders using mass flow controllers (MKS Instruments, Andover, MA), and humidified by bubbling a variable portion of the airstream through water at room temperature (¹⁸O = 4.5, therefore, vapor  14.5), acidified with two drops of 80% (v/v) H₃PO₄. The airflow was split into reference and analysis airstreams, the latter flow range, 800 to 1,500 mL min¹, was passed to a Parkinson "conifer pod" leaf cuvette (PLC) (model PLC3C, ADC Scientific, Hoddeson, UK), and flow was measured via another mass flow controller. Illumination was from a 250 W projector lamp (GEC, Cleveland), passing through a 3-cm depth of water to reduce infrared radiation. Incident radiation on the leaf was controlled by shading with a predetermined number of Miracloth filters (Calbiochem, San Diego). Absolute CO₂ and H₂O concentration in reference and analysis airstreams were monitored alternately via an infrared gas analyzer (model Li-6262, LI-COR, Lincoln, NE).

View larger version (33K): [in this window] [in a new window]   Figure 9.   Arrangement of on-line CO2 trapping and off-line H2O trapping apparatus for continuous flow CO2 isotopic analysis, in conjunction with leaf chamber and gas exchange system.

Isotopic Measurement of CO₂

The outflow of the leaf chamber after passing through the infrared gas analyzer (minimum 700 mL min¹) was split, 100 mL min¹ was pumped first through a dryer (Nafion, Perma Pure, Toms River, NJ), and then a sample loop (0.85 mL) was fitted onto a six-port, two-position valve (Valco Instruments, Houston). CO₂ was trapped at liquid N₂ temperatures for 30 s. After warming to room temperature, the sample was swept with helium carrier gas (120 mL min¹; ultrapure, Gordon Gas and Chemicals, Tel Aviv) through a magnesium perchlorate drying trap and a 2-m packed column (sieve 5A, 80/100 mesh, Alltech, Deerfield, IL) at 60°C. The large peaks of N₂ and O₂ that eluted first from the column were diluted via a gas diluter (Micromass, Manchester, UK), followed by the non-diluted sample CO₂. The gas was introduced into the source of a mass spectrometer (OPTIMA, Micromass) via an open split. ¹³C to ¹²C and ¹⁸O to ¹⁶O isotope ratios were measured from the integrated peak areas of masses 44, 45, and 46 normalized against a 30-s CO₂ reference pulse injected prior to each sample. Sample size was standardized by adjusting the cryogenic trapping time according to the CO₂ concentration in the outflow from the leaf chamber. N₂O was assumed to be constant in air (310 nmol mol¹) and absent from "synthetic" air, so  values were corrected accordingly (Freidli and Siegenthaler, 1988) and expressed in the small delta notation versus Vienna Pee Dee Belemnite (VPDB) for ¹³C and VPDB-CO₂ for ¹⁸O. Precision for repeated sampling of CO₂ was 0.06 (¹³C) and 0.07 (¹⁸O).

Isotopic Measurement of Water Vapor

The remaining airflow from the leaf chamber was passed at positive pressure to a 0.61-cm o.d. stainless steel vacuum line (pressure <1 × 10³ torr) in which CO₂ and water vapor were trapped from the airstream (3 min at 500 mL min¹) in a coil cooled with liquid N₂. After trapping, the line was evacuated and the trap was heated with a flame, distilling both CO₂ and H₂O into a Pyrex side arm immersed in liquid N₂. After quantitative transfer the pyrex tube was flame sealed. The sample was left for CO₂-H₂O equilibrium at constant temperature (29°C, Labline Instruments, Melrose Park, IL) for 72 h. The CO₂ was then dried in a vacuum line with an ethanol trap at 70°C before isotopic analysis on a dual inlet mass spectrometer (MAT 250, Finnigan-MAT, Bremen, Germany). ¹⁸O of water vapor was calculated from that of the CO₂ according to the method of Scrimgeour (1995), correcting for the amount CO₂ and H₂O (calculated from the concentration, flow rate, and time of trapping) and the ¹⁸O of the pre-equilibration CO₂, taken from the corresponding measurement of the continuous flow system. Precision of ¹³C CO₂ and ¹⁸O water vapor was 0.04 and 0.11, respectively.

Experimental Procedure

Light responses were conducted from high to low PPFD (1,200-100 µmol photons m² s¹, 10 intervals) in 21% O₂. Collections of CO₂ for isotopic analyses were carried out for 3 min, while water vapor was trapped continuously (i.e. two samples of CO₂ and one of water were analyzed per light level). Photosynthesis measurements were averaged for the collection period. At the end of the experiment, the portion of leaf inside the cuvette was excised and placed in a 15-mL vacuum container (Becton-Dickinson, Rutherford, NJ) for extraction of leaf water. In addition, three leaf discs (1.8 cm²) were cut from the same leaf, and stored in liquid N₂ for subsequent determination of CA activity. The complete light response analysis (approximately 10 determinations) was first conducted with CO₂ relatively depleted in ¹³C and ¹⁸O (¹³C = 30 and ¹⁸O = 30) to maximize the precision of measurement. Subsequently, ambient air pumped through a 50-L external buffering volume (¹³C  8 and ¹⁸O  0) was used to replicate the experiment. Run-replicate numbers were n = 3 for tobacco (two "depleted" and one ambient air) and n = 2 for soy (one of each).

System 2 (UNUT)

Photosynthesis measurements and cryogenic trapping of CO₂ and H₂O for the experiments on oak were conducted using the CIRAS-1 (PP Systems, Hitchin, UK) and collection system at UNUT, which is described in Gillon and Griffiths (1997). CO₂ isotopic composition was ¹³C = 42, ¹⁸O = 30, with ¹⁸O water vapor approximately = 18. In addition, trapped CO₂ and H₂O were separated via distillation of CO₂ from the mixture using an acetone/liquid N₂ slush at 80°C, as described in Harwood et al. (1998). Precision for dry CO₂ was 0.04 (¹³C) and 0.07 (¹⁸O). Precision for ¹⁸O H₂O determinations was 0.09.

Experimental Procedure

A portion of leaf was placed in the chamber and illuminated for 1 to 2 h before beginning measurements. During sampling, CO₂ and water vapor were cryogenically trapped for 15 min from an airstream of 200 mL min¹, during which time photosynthetic parameters were averaged. This was repeated at various PPFDs (500-100 µmol photons m² s¹, 10-12 steps) to cover the range of CO₂ assimilation from approximately 5 µmol m² s¹ to saturation, allowing the photosynthetic rate to stabilize between each change in PPFD (approximately 20 min). The leaf-to-air VPD was maintained as constant as possible (approximately 1.5 ± 0.2 kPa) throughout the experiment by drying a portion of the reference airstream with Drierite (W.A. Hammond, Xenia, OH). Reference CO₂ was collected between every three to four samples. The complete light response and isotopic analyses were conducted on the same leaf three times, once each at 2%, 21%, and 35% O₂ to check the influence of photorespiration rate (all other experiments at WIS were conducted at 21% O₂).

Leaf Water Heterogeneity

A separate experiment was carried out at WIS to determine the suitability of the Craig and Gordon model to estimate the ¹⁸O of bulk leaf water (_LW). A leaf was placed in the cuvette and left for 1 h (the minimum time for the first measurement in the above light response experiments). A dry CO₂ sample from the leaf chamber was first collected in the stainless steel line by passing the airstream through an additional acetone/liquid N₂ trap at 70°C in the vacuum line. This was used to derive the ¹⁸O CO₂ to be used for equilibration. Next, a water vapor sample from the leaf chamber was collected, as before, and the leaf portion in the cuvette was then excised immediately afterward, and placed in a vacuta