Energy-constrained open-system magmatic processes IV: Geochemical, thermal and mass consequences of energy-constrained recharge, assimilation and fractional crystallization (EC-RAFC)



[1] A wealth of geochemical and petrological data provide evidence that the processes of fractional crystallization, assimilation, and magma recharge (replenishment) dominate the chemical signatures of many terrestrial igneous rocks. Previous work [Spera and Bohrson, 2001; Bohrson and Spera, 2001] has established the importance of integrating energy, species and mass conservation into simulations of complex magma chamber processes. An extended version of the energy-constrained formulation, Energy-Constrained Recharge, Assimilation, Fractional Crystallization (EC-RAFC), tracks mass and compositional variations of melt, cumulates, and enclaves in a magma body undergoing simultaneous recharge, assimilation, and fractional crystallization [Spera and Bohrson, 2002]. Because many EC-RAFC results are distinct from those predicted by extant RAFC formulations, the primary goal of this paper is to present a range of geochemical and mass relationships for selected cases that highlight issues relevant to modern petrology. Among the plethora of petrologic problems that have important, well-documented analogues in nature are the geochemical distinctions that arise when a magma body undergoes continuous versus episodic recharge, the connection between erupted magmas and associated cumulate bodies, the behavior of recharge-fractionation dominated systems (RFC), thermodynamic conditions that promote the formation of enclaves versus cumulates, and the conditions under which magma bodies may be described as chemically homogeneous. Investigation of the effects of continuous versus episodic recharge for mafic magma undergoing RAFC in the lower crust indicates that the resulting geochemical trends for melt and solids are sensitive to the intensity and composition of recharge, suggesting that EC-RAFC may be used as a tool to distinguish the nature of the recharge events. Compared to the record preserved in melts, the geochemical and mass characteristics of solids associated with particular RAFC events may record a more complete view of the physiochemical history of an open-system magma body. The capability of EC-RAFC to track melts and solids creates a genetic link that can be compared to natural analogues such as layered mafic intrusions and flood basalts, or mafic enclaves and their intermediate-composition volcanic or plutonic hosts. The ability to quantify chemical and volume characteristics of solids and melts also underscores the need for integrated field, petrologic and geochemical studies of igneous systems. While it appears that a number of volcanic events or systems may be characterized by continuous influx or eruption of magma (“steady state systems”), reports describing compositional homogeneity for products that represent eruptions of more than one event are relatively rare. In support of this, EC-RAFC results indicate that very specific combinations of recharge conditions, bulk distribution coefficients, and element concentrations are required to achieve geochemical homogeneity during cooling of a magma body undergoing RAFC. In summary, critical points are that EC-RAFC provides a method to quantitatively investigate complex magmatic systems in a thermodynamic context; it predicts complex, nonmonotonic geochemical trends for which there are natural analogues that have been difficult to model; and finally, EC-RAFC establishes the link between the chemical and physical attributes of a magmatic system. Application of EC-RAFC promises to improve our understanding of specific tectonomagmatic systems as well as enhance our grasp of the essential physiochemical principles that govern magma body evolution.

1. Introduction

[2] The geochemical diversity of igneous rocks on Earth results from a complex array of processes, many of which occur in magma storage regions (reservoirs) or during vertical or lateral transport within conduits. The record of these processes is preserved in a spectrum of igneous rocks that ranges from rapidly quenched melts to slowly cooled magmas. Major and trace element and isotopic data collected during the last several decades indicate that first-order magma chamber processes include magma recharge (magma replenishment), assimilation, and fractional crystallization (RAFC). Several quantitative models have been developed that predict the geochemical paths of magmas that undergo RAFC [e.g., O'Hara, 1977; O'Hara and Mathews, 1981; Albaréde, 1995; DePaolo, 1985], and application of these models has led to an increasingly sophisticated understanding of magmatic processes.

[3] In this paper, we build upon previous work that describes the theory and application of Energetically-Constrained Assimilation Fractional Crystallization (EC-AFC), a model which tracks the geochemical, thermal, and mass evolution of magma undergoing concurrent assimilation (of wallrock-derived melt) and fractional crystallization (cumulate formation) in a cooling magma body [Spera and Bohrson, 2001; Bohrson and Spera, 2001]. This model was applied to several natural systems that evolved dominantly by assimilation and fractional crystallization [Bohrson and Spera, 2001]. Abundant evidence suggests that, in general, magma replenishment plays a quantitatively significant role in the generation of the geochemical diversity of igneous rocks in a wide range of settings (e.g., flood basalts, layered mafic intrusions, arcs, mid-ocean ridges, ocean islands). Importantly, it is noted that advection of heat into a standing magma body as well as addition of “fresh” recharge are not independent events. Consequently, the EC-AFC model has been expanded to include the thermal and mass balance implications of magma recharge. The conceptual framework, quantitative development, and assumptions of this new formulation, Energy-Constrained Recharge, Assimilation, Fractional Crystallization (EC-RAFC), are outlined in Spera and Bohrson [2002]. Briefly, the composite RAFC magmatic system includes three sub-systems: an initially pristine (standing) magma body, wallrock that may produce anatectic melt, and a chemically and thermally distinct reservoir of recharge melt. During the RAFC event, recharge and anatectic melts are assumed to flow into and homogenize with standing magma. If the liquidus temperature of recharge magma is higher than the local temperature of the standing magma, a portion of recharge melt, governed by the recharge melt productivity function, solidifies. In EC-RAFC, these solids are called enclaves, and their compositions are governed by fractional crystallization of pristine recharge melt (for a complete explanation of these enclaves [see Spera and Bohrson, 2002]). Cumulates also form in the magma body as a consequence of cooling. The series of coupled differential equations that comprise EC-RAFC self-consistently tracks the thermal characteristics, masses and compositions of enclaves, cumulates, and melt as the sub-systems approach thermal equilibrium. The ability to monitor the mass and compositions of the solids formed during EC-RAFC events is significant because, compared to liquids (which are assumed to be in chemical equilibrium at each point along the RAFC path), solids record the chronological record of incremental changes in composition during RAFC magmatic evolution.

[4] Results illustrated in this paper outline some of the complexity evident in an EC-RAFC composite system and emphasize insight gained by combining information from melts and solids. Among the many possibilities of petrologic relevance that can be examined with EC-RAFC, we highlight the trace element, isotopic, mass and thermal consequences on solids and melt of episodic versus continuous recharge, variations in the thermodynamic properties of the subsystems, variations in the recharge melt input function, recharge-fractionation dominated systems (RFC), conditions that promote the formation of enclaves versus cumulates, and conditions under which magmatic systems may be chemically homogeneous. In addition, the impact recharge has on the efficacy of assimilation is examined. Like EC-AFC, the resultant geochemical paths for solids and melts undergoing EC-RAFC are complex and are often described by non-monotonic element-element, element-isotope trends. A primary goal of this paper is to introduce a range of examples that illustrates this geochemical complexity, particularly because many of the geochemical trends are quite different from those predicted by extant models. The coupled nature of the processes allows specific chemical paths to be associated with defined masses of standing magma and cumulates, recharge magma and enclaves, and assimilant. EC-RAFC therefore provides a tool that links petrologic processes with volume (mass) data of volcanic and plutonic systems. The results presented here emphasize the critical need for integrated field, petrologic and geochemical studies of igneous systems. We suggest that the specificity in geochemical parameter space that results from EC-RAFC simulations will strengthen our ability to decipher the complex interactions among the RAFC sub-systems. Application of EC-RAFC to natural systems is presented in a later study.

2. Episodic Versus Continuous Recharge

[5] EC-RAFC accommodates continuous or episodic recharge of melt of distinct composition and thermal characteristics into the standing magma body for a particular RAFC event [Spera and Bohrson, 2002]. The user defines the total mass of recharge magma (Mro) involved in the RAFC event, as well the cumulative amount of mass addition as a function of temperature (called the recharge melt input function: Mr = f(Tm)). Based in part on geochemical data from temporally well-defined samples, a number of subaerial volcanic systems have been described as characterized by episodic recharge (e.g., Akagi volcano [Umino and Horio, 1998], El Chichon [Tepley et al., 2000], Merapi [Gauthier and Condomines, 1999]). Episodic injection of mafic magma into mid-ocean ridge magma reservoirs is also considered important, as first documented by Dungan and Rhodes [1978] and Rhodes et al. [1979] and as extensively documented by many other investigators since. Geochemical and petrologic data from intrusive complexes such as the Muskox [Irvine and Smith, 1967], the Bushveld [Eales and Cawthorn, 1996], the Rum [Emeleus, 1987; Volker and Upton, 1990] and the Ivrea-Verbano Zone [Clemens-Knott et al., 1999] also have been used as evidence for the occurrence of repeated injections of magma into actively evolving magma chambers. In contrast, some volcanic events, such as the 1759–1774 eruption of Jorullo [Luhr and Carmichael, 1985], the 1943–1952 eruption of Paricutin [Wilcox, 1954], the 1972–1974 Mauna Ulu eruption [Tilling et al., 1987], and the 1968–1985 eruption of Arenal [Reagan et al., 1987] have been described as reflecting “steady state” behavior, where magma is apparently supplied continuously to a sub-volcanic reservoir, although possibly at variable rates. Wadge [1982] made the observation that eruptive phases of a number of volcanoes (e.g., Kilauea, Piton de la Fournaise, Arenal, Santiaguito) reflect “steady state” behavior, which he defined as a linear relationship between cumulative volume of erupted magma and time. There is also the suggestion that activity at some volcanoes, particularly those found in arcs, may be controlled by short time-scale episodic recharge events that are superimposed on a background of longer-term continuous replenishment [Gamble et al., 1999]. Based on estimates of magma supply rates for Krafla, Lakagigar, Kilauea, and Mauna Loa, Takada [1999] made the distinction between rift volcanoes, which are intermittently supplied by larger volumes (1–10 km3) of magma over longer time intervals (102–104 years), and intraplate volcanoes, where the magma supply is continuous although the supply rate may fluctuate.

[6] Such descriptions of and inferences about the nature of magma recharge highlight the complications inherent in quantifying this process. Defining and discerning the differences between continuous and episodic recharge require a clear definition of the timescales over which magma is supplied to the sub-volcanic chamber(s). In addition, the incomplete record of magmatism that is preserved renders distinguishing episodic and continuous recharge events a challenge. Despite these hurdles, developing tools that distinguish these two is a worthwhile pursuit because the style of recharge is likely a function of the mechanics of mantle melting and magma ascent and intrusion dynamics. In addition, distinct indicators of the nature of recharge might allow better integration of geochemical and geophysical data collected at active volcanoes. EC-RAFC can be used as a tool to develop quantitative constraints on the mass and geochemical characteristics of continuously versus episodically recharged magma systems.

[7] Table 1 summarizes input parameters for a case where basaltic magma intrudes lower crust of intermediate composition; the crustal geochemical parameters are similar to those for average lower crust cited in Taylor and McLennan [1985]. To illustrate the consequences of intrusion of recharge magma that is compositionally distinct from pristine magma already making up the magma body, recharge magma, which is intruded continuously or episodically as a function of Tm, is assumed to be more mafic than pristine magma, with less radiogenic Sr and more radiogenic Nd isotope signatures. Sr is modeled to behave compatibly in pristine and recharge magmas but incompatibly during host rock anatexis. Nd is incompatible in all sub-systems. For this set of input parameters, because we have (arbitrarily) chosen recharge magma with initial and liquidus temperatures identical to those of pristine magma, a portion of recharge melt chills upon injection and some enclaves form [see Spera and Bohrson, 2002]. Due to enthalpy transport during recharge, the total masses of wallrock involved in the thermal exchange and of anatectic melt produced are greater than they would have been had no recharge occurred. This is therefore an example where recharge enhances assimilation. An interesting observation related to wallrock anatexis is that it initiates at different temperatures for the continuous versus episodic cases. The local magma temperature at which wallrock reaches its solidus is lower in the continuous recharge case (∼1103°C) compared to the episodic recharge case (∼1119°C). This is because at ∼1119°C, 99% of the recharge magma has been added to the standing magma in the episodic case, whereas only 72% has in the continuous case; the additional latent heat added through crystallization of the episodically recharged magma allows anatexis to initiate at a higher Tm, a result that makes intuitive sense and underscores the coupled nature of recharge and assimilation.

Table 1. EC-RAFC Parameters for Lower Crustal Continuous and Episodic Recharge Cases
Thermal Parametersa
  • a

    Nonlinear parameterization of fa(T), fm(T), and fr(T) used.

  • b

    Continuous recharge adds equal increments throughout entire cooling history, from Tm,o to Teq.

Pristine magma liquidus temperature, Tl,m1320°Ccrystallization enthalpy, Δhm (J/kg)396000 
Pristine magma initial temperature, Tmo1320°Cisobaric specific heat of magma, Cp,m (J/kgK)1484 
Recharge magma liquidus temperature, Tl,r1320°Ccrystallization enthalpy, Δhr (J/kg)396000 
Recharge magma initial temperature, Tro1320°Cisobaric specific heat of recharge, Cp,r (J/kgK)1484 
Assimilant liquidus temperature, Tl,a1100°Cfusion enthalpy, Δha (J/kg)354000 
Assimilant initial temperature, Tao600°Cisobaric specific heat of assimilant, Cp,a (J/kgK))1388 
Total (normalized) mass of recharge magma0.5   
Solidus temperature, Ts950°C   
Equilibration temperature, Teq1020°C   
Recharge Schedule for Episodic Caseb
TemperatureMass of Increment
Compositional Parameters
Pristine magma initial conc. (ppm), Cmo7003510 
Pristine magma isotope ratio, εro0.70350.5130-6.2
Pristine magma trace element distribution Coefficient, Dm1.50.250.1 
Recharge magma initial conc. (ppm), Cr1000205 
Recharge magma isotope ratio, εro1.50.25-7
Recharge magma trace element distribution coefficient, Dr0.70280.51320.1 
Assimilant initial conc. (ppm), Cao23012.71.06 
Assimilant isotope ratio, εao0.71000.5122-12
Assimilant trace element distribution coefficient, Da0.050.250.1 

[8] The geochemical signatures of recharge are distinct, both between the continuous and episodic models and between the recharge and recharge-free (EC-AFC) models (Figure 1). In the cases modeled here, where recharge magma has a Sr isotope ratio that is less radiogenic than that of the pristine magma (i.e., prior to the onset of assimilation), the 87Sr/86Sr of the standing magma decreases. In the case of continuous recharge, the [Sr]-87Sr/86Sr change is smooth whereas in the case of episodic recharge, the change can be described as a step-function (inset, Figure 1). At the Tm where wallrock begins to melt, compared to the episodic case, the continuous recharge case exhibits higher 87Sr/86Sr and lower [Sr] because less recharge magma has been added to the standing magma body. At Teq, the continuous case is therefore characterized by 87Sr/86Sr that is more ‘contaminated’ (i.e., 87Sr/86Sr of the magma is closer to that of the wallrock) than the episodic case.

Figure 1.

Sr (ppm) versus 87Sr/86Sr for episodic and continuous recharge melts for cases presented in Table 1. EC-AFC (no recharge) shown for comparison; where appropriate, all parameters are the same as those in Table 1. (inset) Expanded scale to show distinctions among three cases at relatively high Tm. For all simulations in Figure 1 and all subsequent figures, each symbol represents ∼1°C decrease in Tm.

[9] Although the [Sr] versus 87Sr/86Sr changes associated with recharge (prior to the onset of assimilation) are fairly restricted compared to the total range of these parameters for the entire simulation (to Teq), the range of Tm over which no assimilation occurs is ∼200°C, about 67% of the temperature range of the full simulation (from Tm,o to Teq). This suggests that there may be a distinct record of recharge that is preserved in the cumulates associated with these reservoirs; at the Tm at which wallrock reaches its solidus (i.e., assimilation commences), the total (normalized) mass of cumulates for the continuous case is 0.99 and for the episodic case is 0.88. If eruptions have occurred, this signature of recharge may be preserved in volcanic products as well.

[10] [Nd]-143Nd/144Nd (Figure 2) further illustrates the complex, non-monotonic trends that can derive from EC-RAFC processes. The continuous and episodic recharge models are distinct in Nd concentration-isotope space (Figure 2, inset), as they were in Sr space. [Nd] initially increases because it is modeled as incompatible in all sub-systems. For both recharge cases, the isotope ratio initially increases, reflecting the more radiogenic recharge component. The signature of assimilation eventually dominates both cases, and both [Nd] and 143Nd/144Nd decrease. The concentration decreases because of a dilution effect imparted by fractional melting of an incompatible element (see discussion in Bohrson and Spera, 2001), and the 143Nd/144Nd decreases because the assimilant is less radiogenic. Both recharge cases are different from the recharge-free case, although near Teq, the differences in 143Nd/144Nd and [Nd] among the three examples are subtle.

Figure 2.

Nd (ppm) versus 143Nd/144Nd for episodic and continuous recharge melts for cases presented in Table 1. EC-AFC (no recharge) shown for comparison; where appropriate, all parameters are the same as those in Table 1. (inset) Expanded scale to show distinctions among three cases at relatively high Tm.

[11] Figure 3 illustrates the variations in [Sr] that may be preserved in solids associated with the episodic recharge case presented in Table 1. It is important to appreciate that the enclaves form directly from recharge magma whereas cumulates form from standing magma; therefore, the compositions of the two types of solids are distinct. Instantaneous concentrations reflect the variations that occur as crystals form at each temperature step in the simulation [Spera and Bohrson, 2002]. The record of these compositional variations may be evident in enclaves or cumulates sampled on a small spatial scale. Average concentrations [Spera and Bohrson, 2002] for enclaves, cumulates and all solids reflect the compositions of larger spatial scale (e.g., whole rock) samples. Although Figure 3 implies that documenting magma chamber processes using geochemical data from crystalline bodies may be a complicated task, Figures 4a and 4b underscore the important record these processes preserve. These figures compare the Sr and Nd average concentration-isotope paths of cumulates that may be preserved for the continuous and episodic cases; in detail, these are distinct, and careful sampling and analysis, coupled with use of EC-RAFC, is illuminating.

Figure 3.

Tm versus Sr (ppm) for enclaves, cumulates, and all solids (enclaves + cumulates) for episodic case presented in Table 1. Instantaneous concentrations (closed symbols) reflect [Sr] in new increment of enclave or cumulate formed during temperature decrement dTm. Average concentration (open symbols) reflects [Sr] in all cumulates, enclaves, or total solids. Melt [Sr]-Tm shown for comparison. Instantaneous and average concentration equations for solids presented in Spera and Bohrson [2002].

Figure 4.

Comparison between (a) average Sr concentration (ppm)-87Sr/86Sr, and (b) average Nd concentration (ppm)-143Nd/144Nd in cumulates for episodic and continuous recharge cases presented in Table 1.

3. Geochemical Trends

[12] Several additional observations regarding the geochemical trends of EC-RAFC systems are noteworthy. The [Nd]-[Sr] melt trends for the episodic and continuous recharge cases outlined in Table 1 are illustrative of one type of element-element trend (Figure 5); the EC-AFC case is shown for comparison. In general, prior to onset of assimilation, in the episodic recharge case, [Sr] initially decreases (inset, Figure 5) because more of the element is being removed by fractional crystallization than is being added by recharge. In the case of continuous recharge, [Sr] initially increases because recharge is adding more Sr than is being removed by fractional crystallization. When fractional crystallization dominates, [Sr] decreases in both recharge cases. Nd initially increases in both recharge cases because it is incompatible in pristine and recharge magmas. When anatectic melt is incorporated, Sr initially increases in concentration due to the effects of fractional melting. Eventually, however, because both Nd and Sr are modeled as incompatible in the wallrock, the dilution effect yields decreases in both [Sr] and [Nd]. In the absence of consideration of the effects of partial melting and enclave formation, the non-monotonic nature of these trends might not be recognized as evidence of RAFC processes.

Figure 5.

Sr (ppm) versus Nd (ppm) for episodic and continuous recharge melts for cases presented in Table 1. For comparison, EC-AFC case is included. (inset) Expanded scale to show changes in [Sr] at relatively high Tm.

[13] Sr-Nd and Sr-O isotope trends also reflect the integrated effects of EC-RAFC and emphasize a point made in Bohrson and Spera [2001]. That is, conclusions made regarding the efficacy of particular magma chamber processes based on geochemical trends formulated from models that lack the coupled energy, mass and species conservation approach may lead to incorrect interpretations about the petrogenetic histories of these systems. For example, for the EC-RAFC cases, after the initial increase in 143Nd/144Nd and decrease in 87Sr/86Sr due to recharge, 143Nd/144Nd decreases by only 80–130 ppm while 87Sr/86Sr increases by 5000 ppm (Figure 6). Then, 143Nd/144Nd decreases by up to 270 ppm while 87Sr/86Sr increases by only ∼1000 ppm. The resulting concave downward curve is opposite of that predicted by application of the AFC [DePaolo, 1981] or two-component mixing equations to the same cases (Figure 6). This difference is important because the nature of the concavity has been used to predict ratios of Sr/Nd(melt)/Sr/Nd(contaminant) for a two component system that includes crustal-derived and mantle-derived end-members [DePaolo and Wasserburg, 1979]. In these examples, this ratio is >1. However, for ratios >1, other formulations (e.g., DePaolo [1981] and simple two-component mixing) yield concave upward curves. The key point is that the concavity of these curves can not be interpreted based solely upon initial values of the two end-members; instead, they reflect the integrated effects of assimilation, recharge, and cumulate formation, processes linked through energy conservation. Results of O-Sr isotopes further underscore the problems inherent in using these types of plots to predict characteristics about sub-systems or processes. The EC-RAFC Sr-O isotope curves for these cases are concave upwards (Figure 7), a curvature that has been attributed to source contamination rather than crustal contamination [e.g., Taylor, 1980; James, 1981]. Additional studies using Sr-O isotopes [e.g., Magaritz et al., 1978, Benito et al., 1999], as well as other isotope pairs [e.g., Leat et al., 1991; Molzahn et al., 1996], have made conclusions about source versus crustal level contamination, at least in part, based on the shapes of such isotope-isotope trends. Although the conclusions in these and other studies may be correct, it is clear that EC-RAFC simulations can yield isotope-isotope trends that traditionally have been interpreted to represent source contamination, and therefore reexamination of these cases may be fruitful. It is also important to note that a number of authors have made similar observations regarding the interpretations of Sr-O isotope diagrams [e.g., Davidson et al., 1991; Vroon et al., 1993]: they note that if Sr behaves incompatibly in the magma, then a concave upward trend could be explained by crustal contamination rather than source contamination. While this is correct, it is important to recognize the EC-RAFC yields this concavity even in cases where Sr is compatible in standing magma.

Figure 6.

87Sr/86Sr versus 143Nd/144Nd for episodic and continuous recharge melts for cases presented in Table 1. For comparison, EC-AFC case is included. In addition, an AFC trend (called “classical”), modeled using equations of DePaolo [1981], is included. Where relevant, all parameters are similar to those in Table 1. The r for this case is 0.53, and each symbol represents a decrease in F of 0.05. Note concavity is opposite for EC-RAFC and “classical” AFC.

Figure 7.

87Sr/86Sr versus δ18O for episodic and continuous recharge melts for cases presented in Table 1. For comparison, EC-AFC case is included. In addition, an AFC trend (called “classical”), modeled using equations of DePaolo [1981], is included. Where relevant, all parameters are similar to those in Table 1. The r for this case is 0.53, and each symbol represents a decrease in F of 0.05. Note concavity is opposite for EC-RAFC versus “classical” AFC.

4. Effects of Varying Equilibration Temperature and Recharge Mass Input Characteristics

[14] This section illustrates the importance of incorporating thermodynamic data into quantification of magma chamber processes. The essential observation is that the equilibration temperature (Teq) and the recharge melt input function (Mr = f(Tm)) are fundamental parameters that have impact on the geochemistry of a magmatic system. For example, results from the recharge cases presented in Table 1 (Teq = 1020°C) are compared with cases where all parameters are the same except Teq is ∼100° higher (1120°C). The total mass of wallrock involved in the RAFC event, Mao, is much smaller in the 1120°C cases compared to the 1020°C cases (0.79 versus 1.76, respectively), and therefore assimilation begins at a higher Tm in the 1120°C cases. As a consequence, both 1120°C cases have higher [Sr] when assimilation commences (inset, Figure 8), and at Teq, 87Sr/86Sr is lower than for the 1020°C cases (Figure 8).

Figure 8.

Sr (ppm) versus 87Sr/86Sr for episodic and continuous recharge melts for cases presented in Table 1 (Teq = 1020°C), and for episodic and continuous recharge melts for cases where all parameters are the same except Teq = 1120°C. (inset) Expanded scale to show variations in Sr (ppm) versus 87Sr/86Sr for four cases.

[15] Because the melt productivity function is generally non-linear, [Sr] in the continuous 1120°C case initially increases (inset, Figure 8) due to addition of recharge Sr in the absence of substantive fractional crystallization. When fractionation becomes significant, Sr is removed in greater abundance than is being added by recharge, and [Sr] decreases. (The same effect is observed in the continuous 1020° RAFC case, although the magnitude is smaller). In both cases of episodic recharge, by the Tm at which the first pulse of recharge magma intrudes, fractionation has extracted more Sr than is added by recharge, and [Sr] is therefore lower than the initial value.

[16] Because the recharge melt input function was not modified, a separate effect can be discerned in the 1120°C episodic case. The last pulse of recharge initiates at 1150°C, only 30°C above Teq (compared to 130°C in the 1020°C case). At this Tm, a relatively large normalized mass of recharge magma is intruded (0.30), but due to the dilution effect for Sr that results from fractional melting of the wallrock, the mass of Sr entering the standing magma from assimilation is relatively small. The Sr added from recharge therefore has a proportionally larger effect, and the outcome is a decrease in 87Sr/86Sr at a late stage (Tm close to Teq) in the RAFC event (Figure 8). This demonstrates that the Tm at which a recharge pulse occurs is a critical parameter in modeling an RAFC event. The characteristics of the recharge magma will be more apparent in cases where the mass of Sr being added by anatectic melt is relatively small. In contrast, in the 1020°C case, this effect is not observed because the last pulse of recharge occurs at a Tm at which the dilution effect has not become significant (Figure 8). The inset to Figure 8 also illustrates that, at the onset of wallrock partial melting, the difference in the recharge schedule in the 1120°C case yields a lower [Sr] and a slightly higher 87Sr/86Sr for the episodic recharge case compared to the continuous case. Therefore, at Teq, 87Sr/86Sr of the episodic case is higher than that of the continuous case. The opposite is observed in the 1020°C cases.

5. Recharge-Dominated Systems: RFC

[17] There are particular tectonic settings where, because of the composition of the crust and local stress field (e.g., extensional regime), the magmatic system is dominated by recharge and fractional crystallization (RFC) rather than RAFC. An equally plausible scenario in which RFC would dominate is the case where the anatectic melt extraction efficiency (χ; see Spera and Bohrson [2001]) approaches 0; that is, although anatectic melt is indeed generated in the host, little or none of it is able to mix with standing magma. In the example below, a recharge-dominated system is simulated by artificially setting the assimilant liquidus temperature to an unrealistically high value (∼3000°C) in order to suppress generation of anatectic melt until late (i.e., Tm near Teq) in the RAFC event. It is important to note that even though no anatectic melt is generated or assimilated, the energy balance still is explicitly considered. That is, heat is still extracted from magma to heat wallrock. This is an example where the heat-mass coupling is constrained by the melting characteristics of the wallrock.

[18] The first example of RFC illustrates continuous and episodic cases where more mafic, isotopically less enriched magma recharges a basaltic system located in crust that, for most of the RFC event, does not generate anatectic melt (Figure 9). The equilibration temperature for these cases is ∼1120°C. For comparison, results of the RAFC 1120°C cases (i.e., Tl,a = 1100°C instead of 3000°C) discussed above are included. 87Sr/86Sr initially decreases for both RFC recharge cases, reflecting the less radiogenic 87Sr/86Sr of recharge magma. For most of the magmatic histories of the systems, at the same Tm, the continuous recharge case has higher [Sr] and lower 87Sr/86Sr compared to the episodic case because the added mass of recharge magma is greater. When anatexis commences, both [Sr] and 87Sr/86Sr increase, in response to the effects of fractional melting of wallrock with a more radiogenic Sr isotope signature. However, compared to the 1120°C RAFC cases, the ranges of [Sr] and 87Sr/86Sr for the RFC cases are small because onset of wallrock melting is delayed to a much lower Tm.

Figure 9.

Sr (ppm) versus 87Sr/86Sr for episodic and continuous recharge melts for RAFC cases where all parameters are the same as presented in Table 1, except Teq = 1120°C. For comparison, episodic and continuous RFC cases are shown where Teq = 1120°C and Tl,a = 3000°C. This high liquidus suppresses formation of anatectic melt until relatively low Tm.

[19] The [Nd]-143Nd/144Nd trends (Figure 10) are also profoundly different between the EC-RFC and EC-RAFC cases. The RFC cases show a relatively narrow range of Nd isotope signatures coupled with a large range of [Nd]; this reflects the incompatible nature of Nd in both standing and recharge magmas. Because the total fraction of melting of wallrock that occurs in the RFC case is very small, the dilution effect is not observed in the RFC cases. The RAFC cases describe larger ranges of 143Nd/144Nd but smaller ranges of [Nd].

Figure 10.

Nd (ppm) versus 143Nd/144Nd for episodic and continuous recharge melts for RAFC cases where all parameters are the same as those presented in Table 1, except Teq = 1120°C. For comparison, episodic and continuous RFC cases are shown where Teq = 1120°C and Tl,a = 3000°C.

[20] A separate case examines the behavior of a recharge-dominated system in which the mafic recharge magma is isotopically enriched in 87Sr compared to pristine magma. Such a case might represent recharge of melt derived from a lithospheric source. For the RFC simulations, all parameters are the same as the above RFC cases except that 87Sr/86Sr of the recharge magma is more radiogenic (0.7050). Because a common consequence of AFC is an increase in 87Sr/86Sr, two EC-AFC comparison cases are shown in which Teq is also 1120°C. One has a wallrock bulk distribution coefficient for Sr (DSr) of 0.05 and the other has DSr of 1.5. All other parameters, where appropriate, are the same as the RFC cases. From Tm,o, the continuous RFC case shows a smooth increase in [Sr] followed at lower Tm by a smooth decrease (Figure 11a); this change in trajectory reflects a competition between Sr addition by recharge and Sr removal by fractional crystallization. Changes in [Sr] in the episodic case also reflect this competition, but the result is distinct decreases in [Sr] when crystallization dominates and slight increases or smaller decreases when the pulse of recharge occurs. In both cases, from Tm,o to Teq, 87Sr/86Sr increases. Very different [Sr] patterns are evident for the EC-AFC cases because, initially fractional crystallization is dominant. In the EC-AFC case where DSr is 0.05, when wallrock partial melting commences, [Sr] increases, but at lower Tm, it decreases because of the dilution effect. In the case where DSr is 1.5, [Sr] decreases throughout the simulation. At Teq, 87Sr/86Sr is higher for the EC-AFC cases because the total mass of assimilant is greater. Like the melts, the cumulates also preserve a distinct record of recharge by a magma with relatively high Sr isotope signature (Figure 11b). The critical observation derived from these comparisons is that, even in cases where the recharge magma has 87Sr/86Sr higher than that of the pristine magma, there may be clear geochemical indicators that will allow RFC and AFC processes to be distinguished.

Figure 11.

(a) Sr (ppm) versus 87Sr/86Sr for melt and (b) average Sr (ppm) versus 87Sr/86Sr for cumulates for RFC cases where the Sr isotope ratio of recharge magma (0.7050) is higher than that of pristine magma (0.7035). Melt and cumulate results for two EC-AFC cases are shown for comparison, one in which DSr(wallrock) = 0.05 and the second in which DSr(wallrock) = 1.5.

6. In Situ Evidence of Magma Recharge: Preservation of Enclaves

[21] A number of volcanic (e.g., Crater Lake, Medicine Lake Highland [Eichelberger, 1980], Coso volcanic field [Bacon and Metz, 1984], Monte Arci [Montanini et al., 1994], 1915 Lassen eruption [Clynne, 1999], Mt. Dutton [Miller et al., 1999]) and plutonic (Eagle Lake, California, [Furman and Spera, 1985], Cowra Granodiorite, Lachlan Fold Belt [Waight et al., 2001], Vinalhaven [Wiebe et al., 2001]) systems preserve crystalline inclusions or sheets characterized by a range of textural (e.g., chilled margins, pillow-like morphology, fine-grained) and geochemical traits that suggest they represent recharge of hotter, more mafic magma into a standing, more compositionally evolved magma body. The prevalence of these mafic enclaves or sheets attests to the importance of magma recharge in igneous systems. Textural evidence indicates that, rather than undergoing complete homogenization with host magma, some proportion of the hotter recharge magma can quench in the host. EC-RAFC has the facility to predict not only the composition of melts and associated enclaves (or sheets) but also the masses of each that form under a range of thermal conditions. This ability affords the opportunity to constrain the mass, energetic and chemical characteristics of enclave-bearing volcanic and plutonic systems in a way not previously available.

[22] Episodic and continuous recharge of two cases with different histories of enclave formation are compared; one has recharge magma initial and liquidus temperature (1400°C) that is higher than the initial and liquidus temperature of pristine magma (1320°C) and the second has recharge magma initial and liquidus temperature that is lower (1250°C) than the initial and liquidus temperature of pristine magma. Compared to the 1250°C cases, hotter recharge magma of the 1400°C cases yields a higher mass of enclaves, and the additional latent heat yields involvement of a higher mass of wallrock and anatectic melt. For the 1400°C cases, because the mass of enclaves per temperature interval is larger than that for the 1250°C cases, the mass of recharge melt added to the standing magma body is less; therefore the total mass of cumulates that form during the RAFC event is slightly lower. For episodic and continuous recharge input for the two different cases, Table 2 compares the final masses of wallrock involved in the event, anatectic melt assimilated, enclaves formed, and cumulates formed. These results suggest that enclave formation is favored by recharge magma that intrudes at a temperature higher than the initial temperature of the standing magma body, whereas cumulate formation is favored when recharge magma is at a lower temperature. This result implies that there may be a great deal of information that can be extracted about the characteristics of the recharge magma given tightly constrained field-geochemical studies of volcanic suites and exhumed intrusions.

Table 2. Comparison of Selected Normalized Mass Parameters for Different Initial and Liquidus Temperatures of Recharge Magma
 1400°C, episodic1400°C, continuous1250°C, episodic1250°C, continuous

[23] It is critical to appreciate that distinctions in enclave composition for the cases discussed here may be difficult to detect because the initial composition of each recharge magma increment is equivalent. Thus, the isotope ratios for all enclaves will be the same as the initial isotope signatures of recharge magma, and the [Sr]-[Nd] trends for these cases are similar. Obviously, recharge magma of distinct composition would produce enclaves of distinct composition.

[24] Figure 12a illustrates standing melt [Sr]-87Sr/86Sr trends for the 1250°C and 1400°C episodic and continuous recharge cases; the 1320°C case is excluded for clarity. The 1400°C cases differ from the 1250°C cases because different masses of enclaves are produced, which, in turn, results in different masses of recharge melt entering the standing magma body. The episodic cases differ from the continuous cases because of the coupled nature of the non-linear productivity function for recharge magma and the recharge melt input function (Mr = f(Tm)). The outcome of the integration of these factors is that, by the Tm at which assimilation begins, the episodic 1250°C case has incorporated the most recharge melt and the most recharge Sr; thus, the standing magma has the lowest 87Sr/86Sr and the highest [Sr] (inset, Figure 12a). One consequence of this is that at Teq, the 1250°C episodic case has the least crust-like Sr isotope ratio. At Teq, the 1400°C continuous recharge case is the most crust-like because of the combined effects of fractional crystallization and the relatively small mass of recharge magma added to the standing magma body by the Tm at which anatexis commences. Assimilation commences at the highest Tm in the 1400°C episodic case because of two factors: the first is that by a Tm near the solidus, more recharge magma has been added in the episodic cases than in the continuous cases, and the second is that the specific enthalpy of recharge is higher for Tro = 1400°C compared to the 1250°C case.

Figure 12.

Sr (ppm) versus 87Sr/86Sr for (a) episodic and continuous recharge melts for RAFC cases where Tl,r = Tr,o = 1400°C and Tl,r = Tr,o = 1250°C. (inset) Expanded scale to show variations in Sr (ppm) versus 87Sr/86Sr for four cases, (b) episodic and continuous recharge cumulates for same EC-RAFC cases.

[25] The geochemical records in the cumulates (and total solids) also preserve distinctions between the 1250°C and 1400°C cases. The [Sr]-[Nd] paths are distinct for these cases, and it is important to note that the continuous cases yield an initial increase in the average [Sr] in cumulates (Figure 12b). The [Sr]- 87Sr/86Sr are distinct, and a noteworthy feature of Figure 12b is that early in the cooling history of these magma bodies, [Sr] changes fairly dramatically without large changes in 87Sr/86Sr. In contrast, once assimilation initiates, 87Sr/86Sr changes fairly dramatically, whereas [Sr] is buffered.

7. Petrogenetic Processes Revealed Through Mass Relations

[26] The sizes of plutonic bodies and volcanic eruptions on Earth vary by many orders of magnitude [e.g., Crisp, 1984]. Implicit in this range is information about processes in the associated magma network systems. Because EC-RAFC explicitly tracks the masses of standing melt, cumulates and enclaves, a link can be made between petrogenetic history, composition and volume for particular igneous products. For example, masses of enclaves versus cumulates versus melt for a particular RAFC event can be compared with natural data in order to match compositional signature with mass of product. Such a match would be powerful evidence of the utility of combining these types of data using EC-RAFC to understand magma chamber processes.

[27] Figure 13a illustrates the relationship between Tm and Mm (normalized mass of melt in standing magma body, see Spera and Bohrson, 2002 for explanation) for four continuous recharge cases. Parameters are the same as those in Table 1 with the following exceptions: CASE 1: Tl,r = Tr,o = 1400°C; CASE 2: Tl,r = Tr,o = 1250°C; CASE 3: Teq = 1120°C; CASE 4: Mr = 1. None of the Tm-Mm relationships is monotonic. Each curve increases from an initial value of 1, reflecting the dominance of recharge at relatively high Tm. When fractional crystallization becomes significant, Mm decreases in all cases. The increase of Mm at relatively low Tm reflects onset of assimilation, and thus for these cases, more mass is being added by assimilation and recharge than is being removed by fractional crystallization. Clearly, Teq has a dramatic effect on Mm. For CASE 3, in which Teq = 1120°C, the magma body undergoes the least fractional crystallization, and therefore, at Teq, Mm is the largest. Consistent with this result, the masses of enclaves and cumulates are lowest (Figures 13b and 13c). Enclave formation is favored by high Mr (CASE 4) and by Tl,r (= Tr,o) that is higher than Tm,o (CASE 1). A common example would be injection of high MgO-recharge melt into more evolved basaltic melt. Cumulate formation is favored by high Mr (CASE 4) and Tl,r (= Tr,o) that is lower than Tm,o (CASE 2) because of obvious enthalpy considerations. Using this type of reasoning, relationships among masses of cumulates, enclaves, and melt estimated from field studies may shed light on the characteristics of an RAFC system.

Figure 13.

(a) Tm (°C) versus Mm (b) Tm (°C) versus Men (c) Tm (°C) versus Mct for CASES 1–4. CASE 1 shown by squares, CASE 2 by circles, CASE 3 by diamonds, and CASE 4 by inverted triangles.

[28] Mr/Mct (mass of recharge magma/mass of cumulates) is illustrated in Figure 14a. Like the analogous parameter M*a/Mct in EC-AFC [Bohrson and Spera, 2001], Mr/Mct is not generally constant as a magma body undergoes cooling and crystallization [c.f., DePaolo, 1985; Reagan et al., 1987]. For CASES 1–4 shown in Figure 14a, Mr/Mct varies significantly (∼23 to <1 from Tmo to Teq). The higher values at relatively high Tm reflect input of recharge magma coupled with relatively small amounts of crystallization due to the non-linear nature of the melt productivity functions. As noted in the geochemical results presented for these cases, it is fairly common for the higher Tm stages of the RAFC event to be dominated by recharge, especially at shallower levels where crustal temperatures are relatively low and wallrock can absorb considerable heat before anatexis commences. As fractional crystallization becomes significant at lower Tm, Mr/Mct decreases dramatically.

Figure 14.

(a) Tm (°C) versus Mr/Mct (b) Tm (°C) versus Mct/Mm (c) Tm (°C) versus Ms/Mm for CASES 1–4. (Ms = Men + Mct). Symbols for 4 CASES same as Figure 13.

[29] The ratios Mct/Mm and Ms/Mm (Ms = Men + Mct) for the 4 cases shown in Figures 14b and 14c may also be useful in interpreting mass proportions of products from a magma chamber. These ratios vary from 0 to ∼1–5 and 0 to ∼1–6, respectively. Equilibration temperature has an important effect on these ratios. Compared to the other 3 cases, the Teq = 1120°C case (CASE 3) is melt-dominated throughout its cooling and crystallization history. In the other 3 cases, at higher Tm, the systems are melt-dominated but become and stay solids-dominated at Tm < 1150–1130°C. Thus, for ∼40% of the temperature range, these systems are solids-dominated and the probability of eruption is likely to be relatively low [Marsh, 1981]. Mct/Mm and Ms/Mm > 1 attest to the potential importance solids have in the chemical composition of the crust, and quantifications such as these promise to shed light on the average composition of the crust as well as its compositional structure. The ability to quantify solid versus melt proportions should also yield information about the intrusive to extrusive ratio for a variety of magmatic systems. A possible application of this approach might include determining whether there are systematic differences in cumulate, enclave, and melt masses among systems dominated by RAFC, AFC, RFC or FC or among igneous complexes located in different petrotectonic environments.

[30] Another potentially valuable application of the mass data provided by EC-RAFC involves their use to constrain magmatic systems where cumulates, enclaves and melts (preserved as volcanic rocks) are exposed. Such may be the case for some flood basalt-layered mafic intrusion complexes. Although in practice, application might be limited by exposure and degree of preservation, careful field studies may yield illuminating information about relationships among the masses of these sub-systems. The integration of field and geochemical data proposed here underscores some of the unique and novel capabilities of the EC-RAFC formulation.

[31] The ability to compare the geochemical and mass paths of an RAFC system potentially permits a more sophisticated understanding of the geochemical record preserved by volcanic and plutonic suites. For example, Figure 15 illustrates the 87Sr/86Sr-Mm relationships for CASES 1–4. At higher Tm, there is a relatively large mass of melt characterized by a small range of 87Sr/86Sr. Thus, if some small but constant volume of Mm were to erupt at regular intervals as Tm decreases, then the volcanic record would be characterized by a relatively homogenous Sr isotope signature. In contrast, once assimilation begins, if similar eruptive episodes were to occur, 87Sr/86Sr of the volcanic products would vary by several thousand ppm. At Tm near Teq, the melt erupted would be characterized by a homogeneous but more radiogenic Sr isotope signature than those preserved in highest Tm phases of eruption. The coupling between the characteristics of the magma body and the erupted products can only be qualitatively described here because we have not yet explicitly incorporated eruption into EC-RAFC. However, general patterns can be inferred from the present formulation that may be useful in delineating the RAFC history of particular volcanic suites.

Figure 15.

Mm versus 87Sr/86Sr for CASES 1–4. Symbols for 4 CASES same as Figure 13.

8. The Occurrence of Chemically Homogeneous Magma Bodies

[32] A review of the literature suggests that accounts of compositionally homogeneous eruptive phases (greater than a single eruption) are rare. Even in the cases where eruption is continuous for years (e.g., Jorullo, Arenal), the compositions of the volcanic rocks vary somewhat. For example, the 1759–1774 eruptions of Jorullo Volcano ranged from primitive basalt to basaltic andesite (∼52.1–54.7 wt.% SiO2, 9.3–4.3 wt.% MgO; [Luhr and Carmichael, 1985]) and the 1968–1985 eruptions of Arenal were dominantly basaltic andesite to andesite (∼53.4–56.1 wt.% SiO2, 5.0–3.0 wt.% MgO [Reagan et al., 1987]). In contrast, lavas erupted at Paricutin between 1943 and 1946, which represent ∼75% of the total eruption volume, were considered relatively homogeneous (∼54.6–56.1 wt.% SiO2, 5.6–5.4 wt.% MgO) by McBirney et al. [1987]. The last 25%, erupted between 1947 and 1952, was more varied in composition (∼57.1–60.2 wt.% SiO2, 5.6–3.6 wt.% MgO [McBirney et al., 1987]). Trace element variations in the early, more voluminous phase might also be considered relatively homogeneous, although Sr varied from 537 to 607 ppm and Ba from 315 to 440 ppm. Such descriptions of the compositions of volcanic products, even in examples where the eruptions were continuous, underscore the problems associated with defining chemically homogeneous magma bodies (or parts of magma bodies). Over what timescale does the description apply, and how much latitude is permissible in describing an eruption or eruptive phase as chemically homogeneous?

[33] Table 3 summarizes EC-R(A)FC parameters for a case in which part of the magmatic history might be considered as characterized by magma that is compositionally homogeneous. By defining a high Tl,a (2000°C), the simulation was designed to minimize assimilation because incorporation of anatectic melt tends to drastically change the composition of the magma body. It follows that an initial conclusion based on utilizing EC-RAFC is that typically, compositional homogeneity will be difficult to maintain once anatexis has begun. Figures 16 illustrates a range of approximately 140°C (of the total temperature range of 300°C from Tmo to Teq) which is characterized by RFC (where R is continuous) and where the concentrations of Sr, Nd, Th, and Ni are within 10% of initial concentrations. A narrower compositional range would yield a smaller temperature range over which such compositional homogeneity would be characterized. In order to achieve this result, the recharge magma compositional parameters in this simulation were iteratively modified. The results show a balance between addition of the element by recharge and variation due to fractional crystallization. Sr and Ni concentrations in the recharge magma are higher than those in the pristine magma because these elements are modeled as compatible in all sub-systems. In contrast, the concentrations of Th and Nd are lower in recharge magma than pristine magma because the elements are modeled as incompatible; this relationship allows the recharge magma to have a dilution effect on elements that would otherwise increase in concentration during fractional crystallization. Such concentrations would be consistent with recharge magma that is more mafic than pristine magma.

Figure 16.

Tm (°C) versus trace element (ppm) for melt of continuous recharge case presented in Table 3.

Table 3. EC-R(A)FC Parameters for Continuous Recharge Case that Reflects Chemical Homogeneity
Thermal Parametersa
Pristine magma liquidus temperature, Tl,m1320°Ccrystallization enthalpy, Δhm (J/kg)396000 
  • a

    Non-linear parameterization of fa(T), fm(T), and fr(T) used.

Pristine magma initial temperature, Tmo1320°Cisobaric specific heat of magma, Cp,m (J/kgK)1484 
Recharge magma liquidus temperature, Tl,r1320°Ccrystallization enthalpy, Δhr (J/kg)396000 
Recharge magma initial temperature, Tro1320°Cisobaric specific heat of recharge, Cp,r (J/kgK)1484 
Assimilant liquidus temperature, Tl,a2000°Cfusion enthalpy, Δha (J/kg)354000 
Assimilant initial temperature, Tao200°Cisobaric specific heat of assimilant, Cp,a (J/kgK))1388 
Total (normalized) mass of recharge magma0.5   
Solidus temperature, Ts950°C   
Equilibration temperature, Teq1020°C   
Compositional Parameters
Pristine magma initial conc. (ppm), Cmo7003510100
Pristine magma isotope ratio, εmo0.70350.5130--
Pristine magma trace element distribution coefficient, Dm1.
Recharge magma initial conc. (ppm), Cro100071115
Recharge magma isotope ratio, εro1.50.25--
Recharge magma trace element distribution coefficient, Dr0.70280.51320.11.5
Assimilant initial conc. (ppm), Cao23012.71.0610
Assimilant isotope ratio, εao0.71000.5122--
Assimilant trace element distribution coefficient, Da1.

[34] Once assimilation becomes important, the concentrations of all of these elements vary substantially. The key point is that, based upon results using EC-RAFC, achieving compositional homogeneity is a challenging task because of the integrated effects of mass, species and energy conservation and the effects of partial melting, fractional crystallization and recharge. It is likely that the assumption of complete homogenization at each step in the EC-RAFC event maximizes the potential for compositional homogeneity in the theoretical magma body; the existence of compositionally zoned volcanic products suggests that this assumption is not always valid. Thus, an important prediction of the EC-RAFC formulation is that compositionally homogeneous magma bodies are likely to be relatively rare. This prediction is, in general, supported by data collected from natural systems.

9. Conclusions

[35] The Energy-Constrained Recharge, Assimilation, Fractional Crystallization (EC-RAFC) formulation tracks the mass, energy (enthalpy and temperature), trace element and isotopic composition of anatectic melt, magma body melt, cumulates generated by fractional crystallization and enclaves formed by chilling of recharge melt injected into an evolving magma body. The magma body, which represents one part of a three component system amenable to thermodynamic characterization, undergoes simultaneous recharge, assimilation and fractional crystallization. Results of selected simulations clearly illustrate distinctions in composition that arise between systems characterized by episodic versus continuous recharge. Clear compositional differences in evolutionary trends in limiting cases (RFC or AFC) compared to the more general RAFC case are also apparent. Similarly, thermal conditions that favor formation of enclaves versus cumulates are easily explored. Injection of high specific enthalpy recharge melt into lower enthalpy standing melt results in enclave formation at the expense of cumulate formation. In contrast, injection of recharge magma of similar or less specific enthalpy results in a wave of cumulate formation with far less (or no) enclave formation. The quality of the correlations between the mass of added recharge melt (Mro) and the extent of anatexis (M*a) depends on thermodynamic parameters and initial conditions. Based on EC-RAFC simulations, it appears that chemical homogeneity during cooling and crystallization of a magma body is favored when assimilation is negligible and when particular combinations of element concentrations and partition coefficients in recharge and pristine magma are maintained. These results are consistent with the small number of reported examples of phases of volcanic eruption or plutons that are chemically homogeneous. Because the composition and masses of melt and solids (cumulates and enclaves) are monitored by EC-RAFC, quantitative petrogenetic models describing the formation of any magmatic system can be investigated. Application of the formulation holds promise for increasing the understanding of magmatic systems as diverse as flood basalts, arc volcanoes, layered mafic intrusions, and granitic batholiths. The ability of EC-RAFC to predict mass and compositional relationships for individual magmatic systems also underscores the importance of well-constrained field-geochemical studies. For information about the availability of downloadable EC-RAFC code, go to A computer code for EC-AFC is available at the same website.


[36] We acknowledge the programming efforts of Guy Brown, who rendered our dense notations into functional code. We also thank Vincent Salters, an anonymous reviewer, guest editor Hubert Staudigel and editor Bill White for comments that helped improve the manuscript. Support for this project was provided by NSF EAR94-18720 (FJS), NSF EAR96-14381 (WAB). FJS acknowledges support from the U. S. Department of Energy DE-FG03-01ER-15210 and WAB acknowledges support from the Office of Graduate Studies and Research, Central Washington University.