 Research article
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Diffusioncontrolled growth and degree of disequilibrium of garnet porphyroblasts: is diffusioncontrolled growth of porphyroblasts common?
Progress in Earth and Planetary Science volume 2, Article number: 25 (2015)
Abstract
Ratelimiting processes and the degree of disequilibrium during metamorphic mineral growth are key controls on the rate of dehydration and hydration in the Earth’s crust. This paper examines diffusioncontrolled growth and the degree of disequilibrium of garnet porphyroblasts in the Tsukuba metamorphic rocks of central Japan. The analyzed porphyroblasts have irregular and branching morphologies with clear diffusional haloes, indicating that they grew in a diffusioncontrolled regime. Mathematical analysis shows that the dominant wavelength of the interface of a garnet porphyroblast is dependent on the extent of supersaturation (Δζ), which is an index for the degree of disequilibrium. Using the calculated upper and lower limits of the dominant wavelength, the value of Δζ is estimated to be 0.05 × 10^{−1}–0.16, which corresponds to a Gibbs free energy (ΔG _{ r }) overstep of 0.9–27 kJ per mole of garnet (12 oxygen atoms) and a temperature overstep (ΔT) of 1.7–50 °C. Using the average value of the dominant wavelength, the following results are obtained: Δζ = 0.15 × 10^{−1}, ΔG _{ r } = 2.7 kJ per mole of garnet, and ΔT = 5 °C. These values bring into question the importance of diffusioncontrolled growth of garnet porphyroblasts, as highly irregular and branching garnet porphyroblasts are rare in most metamorphic belts. After significant overstepping for the nucleation of garnet, the garnet porphyroblasts grow at a high degree of disequilibrium. However, a high degree of disequilibrium under diffusioncontrolled growth would be characterized by diffusional instability. The results indicate that garnet porphyroblasts that lack an irregular and branching morphology may grow at a high degree of disequilibrium under interfacecontrolled growth, provided they are set in a medium where the diffusion and supply of constituent elements are sufficient, such as a sufficient volume of metamorphic fluid.
Background
Ratelimiting processes and the degree of disequilibrium of a metamorphic reaction are crucial factors in the devolatilization and/or hydration of the Earth’s crust. The release and consumption of fluids, such as waterrich fluids and melts, have a critical influence on the evolution of mountain building and the transport of energy and materials in the crust. Many studies have assessed the ratelimiting processes for metamorphic reactions (e.g., Ague and Carlson 2013, Walther and Wood 1984). The following three types of ratelimiting processes have been recognized (e.g., Fisher 1978): 1) interfacecontrolled, 2) diffusioncontrolled, and 3) heatflowcontrolled. The formation of garnet is one of the most common devolatilization reactions in the crust (e.g., Ague and Carlson 2013), and diffusioncontrolled processes are widely applied to garnetforming reactions, including the nucleation and growth of the garnet (e.g., Carlson 1989) and Ostwald ripening (Miyazaki 1991, 1996). Although Carlson (1989) and Miyazaki (1991) both assumed a diffusioncontrolled process, the degree of disequilibrium differed in their models. In particular, the degree of disequilibrium for the nucleation and growth model is much higher than that for Ostwald ripening. Even if the ratelimiting processes were governed by diffusion, the degree of disequilibrium should directly affect the reaction rate and the patterns of metamorphic textures. The growth of a metamorphic mineral at a low degree of disequilibrium (i.e., a system close to equilibrium, implying a small overstep from the equilibrium temperature and a low degree of supersaturation for the metamorphic reaction) may result in an equigranular metamorphic texture because interfacial energy becomes an important control on crystal morphology and size. On the other hand, growth at a high degree of disequilibrium with a limited number of nuclei may result in a porphyroblastic texture. However, diffusioncontrolled growth of a mineral at a high degree of disequilibrium is likely to involve diffusional instability and may lead to highly irregular and branched morphologies. In this paper, I examine the diffusional instability of garnet porphyroblasts (Tsukuba metamorphic rocks, central Japan) that grew in a diffusioncontrolled regime.
Methods
Identification of a texture characteristic of diffusioncontrolled growth
Diffusioncontrolled growth is the result of the sluggish diffusion of the elements required for growth of the product of the reaction and is characterized by the presence of a depleted zone that formed around the growing product (Fig. 1). It is assumed that a uniform medium existed initially before nucleation of the product. After nucleation occurs, the region surrounding the reaction product will supply elements to the growing product. Although a uniform medium continues to exist outside the region immediately surrounding the growing product, the concentration of elements required for growth is reduced in the immediate surroundings by the diffusion of those elements to the product. If the reactants needed for the growth of the product exist in the surrounding region, they should dissolve selectively. Therefore, it is expected that the reactants should be remarkably depleted in the immediate surroundings of the growing product. The resulting depletion zone contains the characteristic texture for diffusioncontrolled growth. Therefore, a search for a zone that is depleted in the reactants of a garnetforming reaction is the first step towards estimating the degree of disequilibrium associated with diffusioncontrolled growth of garnet porphyroblasts.
Mathematical analysis of diffusional instability
Diffusional instability should occur when a product grows by a diffusioncontrolled process. For example, if the small tip of a growing product occurs in a diffusional medium, the concentration gradient around the tip becomes larger compared with the area around the flat surface of the product (Fig. 2). The growth rate of the tip will be higher than the flat surface because the influx of any reactionlimiting component (RLC) (Kelly et al. 2013a) is proportional to the concentration gradient of the RLC in the diffusional medium (see Fig. 2). This implies that diffusional instability is always to be expected under diffusioncontrolled growth, and that diffusional instability will lead to highly branched textures that emerge from very small perturbations. However, interfacial energy may offset this type of instability.
Assuming the growth of a spherical product (such as a garnet porphyroblast) with radius R _{ g } in a diffusional medium, and a mass balance at the spherical surface, where a growth rate dV/dt = 4πR _{ g } ^{2} (dR _{ g }/dt) is proportional to the diffusional flux J = –D (∂c/∂r), the diffusioncontrolled growth rate becomes:
where D is the diffusion coefficient of the RLC in the medium, C is the concentration of the RLC in the product, and r, c, and c _{ R } are the distance from the center of the product, the concentration of the RLC in the diffusional medium, and the equilibrium concentration of the RLC at the interface of the product with radius R _{ g }, respectively. Assuming the Gibbs–Thomson effect, the concentration c _{ R } is defined as follows:
where Γ _{ D } = γΩ/RT is the capillary length, and γ and Ω are the interfacial energy and the molar volume of the product, respectively. The R is the gas constant and T is the temperature. The c _{ eq } is the equilibrium concentration of the RLC in the medium at the interface of a product with a flat surface. The c _{ R } is higher than c _{ eq } due to the Gibbs–Thomson effect. When concentration c only depends on the radial component, the diffusion equation in polar coordinates becomes ∂c/∂t = D (∂^{2} c/∂r ^{2} + 2/r (∂c/∂r)). Assuming steadystate conditions (i.e., ∂c/∂t = 0), the solution of c = c _{ m } – (c _{ m } – c _{ R }) (R _{ g }/r) is obtained, where c _{ m } is the concentration of the RLC at a long distance from the product interface. The solution satisfies c _{ r=∞ } = c _{ m } and c _{ r=Rg } = c _{ R }. Using Eqs. 1 and 2, and assuming steadystate diffusion around the spherical product of radius R _{ g }, the growth rate dR _{ g }/dt becomes (e.g., Lifshitz and Slyozov 1961):
where Δζ is the supersaturation. The Δζ is defined as follows:
Mullins and Sekerka (1963) presented a mathematical analysis of diffusional instability, and they introduced a small perturbation δ on a spherical product with radius R _{ g }. The distorted interface of the sphere then becomes:
where r is the distance from the center of the product to the interface, and Y _{ lm } (θ,φ) is a spherical harmonic function. The l (degree) and m (order) of the spherical harmonic function are integers, where l > 0 and –l ≤ m ≤ l. The wavelength of the perturbation decreases with increasing l. For example, the wavelength of the small perturbation of Y _{ 30 } (θ,φ) is three (Fig. 3). The following equation describes the relationship between degree l and wavelength λ _{ l } (Mullins and Sekerka 1963):
A growth rate dδ _{ l }/dt for a small perturbation δ _{ l } for the degree l is obtained by assuming steadystate diffusion around the growing product with radius R _{ g }, as follows (Mullins and Sekerka 1963):
The first term in the bracket on the righthand side of Eq. 7 represents an acceleration of the perturbation due to diffusional instability, and the second term shows a reduction in the perturbation due to interfacial energy. Together, these two terms govern the evolution of the small perturbation. Using Eq. 7, the growth rate dδ _{ l }/dt of the small perturbation can be obtained as a function of the degree l. Using the relationship between l and λ _{ l } (Eq. 6), Fig. 4 implies that the growth rate has a maximum value at l _{max}. The l _{max} is defined as follows (Mullins and Sekerka 1963):
Equations 6 and 8 show that the dominant wavelength λ _{max} (=2πR _{ g }/l _{max}) can be directly extracted from the supersaturation Δζ. In reverse, this means that the observed dominant wavelength of the product interface should be linked to the supersaturation.
The relative growth rate of a small perturbation for a sphere with radius R _{ g } is calculated using Eqs. 3 and 7, as follows:
where R _{ l } is the critical radius of the diffusional perturbation of the degree l, and R _{ c } is the critical radius for Ostwald ripening. Under the condition of R _{ g } > R _{ c }, the perturbation of the degree l will grow when R _{ g } > R _{ l }. In contrast, the perturbation of the degree l will disappear when R _{ g } < R _{ l }. Because Eq. 9 becomes zero at l = 1, the condition R _{ g } > R _{ l=2} will lead to unstable growth, causing an irregular shape to form instead of a sphere. On the other hand, when R _{ g } < R _{ l=2}, a compact spherical morphology becomes stable. Assuming a growth rate dδ _{ l }/dt = 0 and R _{ g } = R _{ l } in Eq. 7, R _{ l } becomes:
Similarly, R _{ c } is given by Eq. 3, as follows:
Combining Eqs. 10 and 11, R _{ l } can be written as follows:
Although R _{ c } has a very small value, Eq. 12 implies that R _{ l } becomes very large for a large l.
Measurement of the garnet morphology
Equations 6 and 8 imply that the supersaturation Δζ for diffusioncontrolled growth can be directly obtained from the dominant wavelength λ _{max} of the interface of the growing product. Measurements of the dominant wavelength of garnet produced by diffusioncontrolled growth were performed by measuring the radius of local curvature of the garnet interface (method 1), and by measuring the power spectra of the garnet interface (method 2).
In method 1, the local curvature k is characterized by the number of particles n _{ l } belonging to a circle with radius r _{ s } (Koshizuka 2005). Here, the local curvature k = 1/r _{ r } is calculated by counting the pixels included in a circle with radius r _{ s } (Fig. 5), as follows:
where n _{ i } is the number of pixels within circle i with radius r _{ s }. The n _{ 0 } represents n _{i} for a flat surface. The r _{ s } ranges from 3.1 to 21.1 pixel units and is adjusted to obtain the largest value of local curvature at a given position on the garnet interface. The calculated local curvatures are calibrated, as a local curvature of a circle with radius r becomes 1/r. The calibration length ranges from r = 2 to 120 pixel units. The calibrating local curvatures for circles with radii from r = 2 to 120 pixel units are basically identical to the inverse of the radii of the target circles (=1/r) (Fig. 6). The dominant wavelength of the garnet interface is clearly larger than twice the length of the radius of the local curvature because the wavelength of a tip is always larger than twice the length of the radius of the enveloping circle at the tip. Hence, the lower limit for the dominant wavelength is twice the length of the radius of the local curvature.
Method 2 uses interface positions measured from the garnet barycenter to estimate the power spectra of the interface morphology. Before the measurement of interface positions, inclusions in the garnet are filled. The measured interface positions are represented by the angle θ and the distance r from the barycenter (Fig. 7). A θ value of 0° is defined as downward in the vertical direction from the barycenter, and the value of θ increases counterclockwise. The number of sampling points is 1024 or 2048 between θ = 0° and 360° around the barycenter. The power spectra f(θ) was estimated using the fast Fourier transform (FFT) of the distance r as a function of θ. The dominant spectra obtained in degrees are converted to lengths by the mean radius from the barycenter of the garnet. The FFT cannot be applied to overhanging parts of the interface; therefore, only nonoverhanging parts were used. This treatment leads to a lack of information on the power spectra in overhanging parts, which have many undulations (Fig. 7). Therefore, the estimates of the power spectra for shorter wavelengths are underestimated in this paper. Here, I used the dominant wavelength obtained from method 2 as the upper limit. Hence, the true value of the dominant wavelength should lie between the values obtained from methods 1 and 2.
Tsukuba metamorphic rock sample
The sample analyzed for this study was collected from the highgrade part of the Late Cretaceous low pressure–high temperature (LP–HT) Tsukuba metamorphic rocks that form an eastern extension of the Ryoke metamorphic complex. The locality of the sample (number Ma248a) was described by Miyazaki (1999). The protoliths of the Tsukuba metamorphic rocks were mudstones and sandstones of an accretionary complex of Late Jurassic to earliest Cretaceous age (Miyazaki et al. 1996). The Tsukuba metamorphic rocks were intruded by Late Cretaceous to earliest Paleogene granitic plutons. The metamorphic grade increases from southeast to northwest.
Based on the mineral assemblages, the pelitic metamorphic rocks can be assigned to the biotite and sillimanite zones. The mineral assemblage of the biotite zone rocks is biotite + muscovite + quartz + plagioclase ± andalusite, whereas the sillimanite zone rocks contain Kfeldspar + sillimanite + biotite + quartz + plagioclase ± cordierite ± garnet. The boundary between the biotite and sillimanite zones is defined by the dehydration reaction of muscovite and quartz, which produces Kfeldspar, sillimanite, and water. The sample analyzed for this study belongs to the highgrade part of the sillimanite zone and contains Kfeldspar + garnet + cordierite + biotite + plagioclase + quartz + sillimanite. The average pressure–temperature (P–T) conditions of samples previously studied from the locality of the present sample are P = 0.34 ± 0.1 GPa and T = 642 ± 16 °C (Miyazaki 1999).
Based on digital maps showing the distribution of minerals, as compiled from Xray intensity maps of Na, K, Mn, Fe, and Al, the mineral mode of the sample is 57 % quartz, 22 % Kfeldspar, 8 % plagioclase, 6–7 % biotite, 4–5 % cordierite, 1–2 % garnet, and <1 % sillimanite (Miyazaki 2001). Kfeldspar, biotite, plagioclase, and quartz are distributed randomly as matrix minerals with diameters of 50–60 μm and do not occur as porphyroblasts (Miyazaki 2001). Because of its low abundance in the sample, it is unclear if sillimanite also has a random distribution in the matrix.
Cordierites occur as porphyroblasts (diameter ≤1 mm) and exhibit irregular shapes. The porphyroblasts have a highly branched texture that may have been formed by diffusionlimited aggregation (DLA). The diffusion of Al may be ratelimiting for DLAlike cordierite porphyroblast growth (Miyazaki 2001). Comparisons of the morphologies and fractal dimensions of the cordierites with those of DLA indicate that formation of the cordierite porphyroblasts can be modeled as a DLA process (Miyazaki 2001). A finitesized growth fluctuation, induced by a random distribution of matrix minerals, is amplified by the diffusional field and results in a DLAlike pattern of porphyroblast growth. Hence, diffusioncontrolled growth within a random matrix field is essential for the formation of DLAlike patterns in cordierite porphyroblasts (Miyazaki 2001).
Garnets occur as porphyroblasts (diameters ≤1 mm) and have irregular shapes (Figs. 8 and 9). Biotite is depleted around garnet porphyroblasts (Fig. 8). Quartz, cordierite, Kfeldspar, and plagioclase are present in the depletion zone but biotite is rare or has smaller crystal sizes compared with biotite outside the depletion zone. Cordierite in the depletion zone is much smaller in size than the porphyroblastic cordierite (Fig. 9b). The number and size of Kfeldspar grains in the depletion zone are also small compared with those outside the depletion zone (Fig. 9a). Sillimanite does not occur in the depletion zone.
The chemical compositions of the constituent minerals were given by Miyazaki (1999). The garnet contains about 7 wt% MnO (73 % almandine, 16 % spessartine, 9 % pyrope, and 2 % grossular). Compositional zoning of MnO, FeO, MgO, and CaO was not detected (Fig. 9), but slightly higher MnO contents occur rarely at the tips on the outer rims of garnet porphyroblasts. Biotites are made up of the components phlogopite (41 %), eastonite (26 %), Tibiotite (17 %), and muscovite (16 %). The endmember formulae of these components are phlogopite (KM_{3}AlSi_{3}O_{10}[OH]_{2}), eastonite (KM_{2}Al_{2}Si_{2}O_{10}[OH]_{2}), Tibiotite (KM_{1.5}TiAl_{2}Si_{2}O_{10}[OH]_{2}), and muscovite (KAl_{3}Si_{3}O_{10}[OH]_{2}) (e.g., Ikeda 1990), where M represents the divariant cations of Mg, Fe, and Mn. The cordierites consist of hydrous cordierite (50 %) and Fecordierite (50 %). The Kfeldspar contains 20 % of the albite component.
Garnetforming reaction and reaction entropy
To estimate the degree of disequilibrium, the garnetforming reaction in the sample should be identified, which is crucial for evaluating the extent of reactant depletion in the region surrounding garnet porphyroblasts. In addition, the reaction entropy ΔS _{ r } for the garnetforming reaction is required to estimate the extent to which the Gibbs free energy ΔG _{ r } was overstepped. Because dG = (∂G/∂P) dP + (∂G/∂T) dT + (∂G/∂N) dN, where P is pressure and N is the number of molecules, the Gibbs free energy depends only on (∂G/∂T) = −S at constant pressure and bulk composition. Therefore, the reaction entropy for the garnetforming reaction is required to estimate the overstepping of Gibbs free energy at constant pressure and bulk composition. The ΔG _{ r } is calculated as follows:
where ΔT is the temperature overstep from the equilibrium temperature. Equation 15 shows that a smaller reaction entropy will yield a larger temperature overstep at a constant overstepping of Gibbs free energy.
For simplicity, the garnetforming reaction for the studied sample is represented by the following univariant reaction in the K_{2}O–MgO–FeO–Al_{2}O_{3}–SiO_{2}–H_{2}O system:
The model compositions used for the minerals are listed in Table 1. In this system, garnet, biotite, and cordierite are treated as almandine–pyrope, phlogopite–annite, and hydrous cordierite–Fecordierite solid solutions, respectively, with the X _{ Fe } of these minerals adjusted to the X _{ Fe } observed in the sample. The other minerals are treated as pure phases. The spessartine component in garnet and the albite component in feldspar make minor contributions to the reaction entropy. However, the Tibiotite, eastonite, and muscovite components in the biotite may contribute significantly to the reaction entropy by increasing the stoichiometric coefficient of water in the garnetforming reaction. Increasing these components increases the reaction entropy. To obtain the minimum reaction entropy, I used a phlogopite–annite solid solution for biotite and the maximum contribution from the hydrous cordierite component.
Using the standardstate entropy and heat capacity of the endmember minerals (Holland and Powell 2011) and assuming ideal mixing for garnet, biotite, and cordierite solid solutions, the reaction entropy at 642 °C becomes 542 J/K for the formation of 1 mole of garnet (12 oxygen atoms). The reaction entropy is also a function of temperature at constant pressure. Here, I assumed that the change in reaction entropy between 642 and 742 °C is not significantly different compared with the reaction entropy at 642 °C. For example, the reaction entropy is 541 J/K at 700 °C and 540 J/K at 742 °C.
Results
Diffusional haloes around garnet porphyroblasts
The garnetforming reaction (Eq. 16) shows sillimanite, biotite, and quartz as the reactants and garnet, cordierite, Kfeldspar, and water as the products. As shown in Fig. 8, biotite is scarce in the area surrounding the garnet porphyroblasts. Biotite is the most important reactant that supplies Al, Fe, and Mg to a growing garnet crystal. Therefore, the observed depletion of biotite around garnet porphyroblasts provides direct evidence for diffusioncontrolled growth. The depletion zone is recognized as diffusional haloes around garnet porphyroblasts. Sillimanite is also an important reactant that supplies Al to garnet, but it is scarce in the matrix. Because sillimanite is typically found farther away from the garnet, the depletion zone of sillimanite around the garnet is much more difficult to identify than the biotite depletion zone.
Cordierite and Kfeldspar are products of the garnetforming reaction. The cordierite crystals in the depleted zone are much smaller than the porphyroblastic cordierite. The number and size of Kfeldspar grains in the depletion zone are also smaller than outside the depletion zone. These observations indicate that growth of cordierite and Kfeldspar within the depleted zone was suppressed in comparison with growth of cordierite porphyroblasts and Kfeldspar matrix minerals outside the depletion zone.
Dominant wavelength and supersaturation
Histograms of the radii of the local interface curvature of seven garnets within the sample show a peak around 30–70 μm (Fig. 10). This peak corresponds to the highest frequency of radii measured from local curvatures of undulations in the irregular garnets. As mentioned above, the wavelengths of these undulations are larger than twice the radius of the local curvatures. Using the midrange values of the histogram peaks for the seven garnet crystals, the calculated average radius of the local curvatures is 43 ± 4.5 μm (Table 2). Therefore, the dominant wavelength obtained from method 1 should be greater than 86 μm.
The power spectra of the interface of irregular garnets show a broad maximum around 150–700 μm (Fig. 11). Using the midrange values of these maxima, the calculated average value is 489 ± 88 μm (Table 2). Therefore, the dominant wavelength obtained from method 2 should be smaller than 489 μm.
Given a dominant wavelength between 86 and 489 μm, interfacial energy γ = 1.0 J/m^{2} (Miyazaki 1991), molar volume Ω = 1.2 × 10^{−4} m^{3}/mole (Miyazaki 1991), T = 642 °C, and a capillary length Γ _{ D } = γΩ/RT = 1.58 × 10^{−5} mm for garnet, Eqs. 6 and 8 yield a supersaturation Δζ of 0.05 × 10^{−1}–0.16 for garnet using the observed average garnet radius of 644 μm. By decreasing the supersaturation Δζ, the dominant wavelength becomes larger (Fig. 12). Taking the average value of the lower and upper boundaries for the dominant wavelength (288 μm; see Table 2), a Δζ value of 0.15 × 10^{−1} is calculated. The average value of the dominant wavelength is consistent with the crude spacing of undulations along the irregular interface of garnet porphyroblasts (Figs. 8 and 9).
Gibbs free energy and temperature oversteps
The calculated supersaturation can be used to determine the magnitude of Gibbs free energy and temperature oversteps. The sample retains the reactant mineral assemblage of sillimanite + biotite + quartz in areas distant from the garnet porphyroblasts. Conversely, the product mineral assemblage of Kfeldspar + cordierite occurs proximal to the garnet porphyroblast. Assuming that reactants far from the garnet porphyroblast are locally in equilibrium with the diffusive medium, the chemical potential difference Δμ _{dissolution} for dissolution of a reactant is
Here, μ _{reactant} is the chemical potential of the reactant and μ _{IGM} is the chemical potential of the chemical species dissolved in the intergranular medium. The μ _{IGM} is expressed as follows:
where m _{ i } is the number of moles of chemical species i exclusive of the RLC that enter or leave the intergranular fluid in the reactantdissolution and productprecipitation reactions, μ _{ i } is the chemical potential of chemical species i exclusive of the RLC, m _{RLC} is the number of moles the RLC, and μ _{RLC} is the chemical potential of the RLC. The summation in Eq. 18 excludes the chemical potential of the RLC. In Eq. 19, the \({\mu}_{\mathrm{RLC}}^0\) is the chemical potential of the pure (unmixed) RLC and X _{RLC,m } is the mole fraction of the RLC in the intergranular medium at a site distant from the garnet porphyroblast. Equation 19 assumes ideal mixing of the RLC in the intergranular medium. In the diffusioncontrolled regime, X _{RLC,m } varies between areas proximal to and distant from the garnet porphyroblast. Hence, Eq. 17 becomes
Assuming the products around the garnet porphyroblast are locally in equilibrium with the diffusive medium, the chemical potential difference Δμ _{precipitation} for a product surrounding the garnet porphyroblast is
where μ _{product} is the chemical potential of the product and X _{RLC,grt } is the mole fraction of the RLC around the garnet porphyroblast. Because garnet growth is controlled by the slowest diffusion of the RLC, the chemical potential differences of the intergranular medium between the areas proximal to and distant from the garnet porphyroblast depend on the chemical potential of the RLC in the medium. This constancy indicates that μ _{IGM0} in Eq. 20 has the same value as in Eq. 21. Using Eqs. 20 and 21, the mole fractions of the most sluggish component of the RLC become
From Eqs. 4, 22, and 23, the supersaturation Δζ becomes
where a is a constant for converting from a mole fraction to concentration, and ΔG _{ r } = μ _{reactant} − μ _{product} is the Gibbs free energy for the garnetforming reaction (Eq. 16). The ΔG _{ r } in this study is equivalent to reaction affinity A (e.g., Pattison et al. 2011) and ΔG _{ r } is zero at the equilibrium temperature. I assumed that the RLC is Al, corresponding to m _{RLC} = 24, and that the equilibrium temperature is T = 642 °C. Using Eq. 25, the supersaturation Δζ of 0.05 × 10^{−1}–0.16 yields a ΔG _{ r } of 0.9–27 kJ per mole of garnet (12 oxygen atoms). The average Δζ of 0.15 × 10^{−1} yields a ΔG _{ r } of 2.7 kJ per mole of garnet.
Using Eq. 15, ΔG _{ r }, and the reaction entropy ΔS _{ r } of 542 J/K per mole of garnet for the garnet reaction, a temperature overstep ΔT of 1.7–50 °C is calculated using the lower and upper boundaries of the dominant wavelength. When the average dominant wavelength is used, a ΔT of 5 °C is calculated.
Discussion
Estimates of the degree of disequilibrium for the garnetforming reaction have been reported in previous studies. Pattison and Tinkham (2009) evaluated the temperature and Gibbs free energy oversteps for a garnetforming reaction in the Nelson aureole (British Columbia) using discrepancies between phaseequilibrium modeling and field observations of the location of the garnet isograd. This approach yielded ΔT = 30 °C and ΔG _{ r } = 4.8 kJ per mole of garnet. The degree of disequilibrium for the Nelson aureole is similar to that calculated for the sample in this study. However, the garnet porphyroblasts in the Nelson aureole are euhedral rather than irregular and branching in the case of the garnets from the Tsukuba metamorphic rocks. Kinetic modeling based on interfacecontrolled nucleation and growth was used to explain the formation of the garnet in the Nelson aureole (Gaidies et al. 2011). On the other hand, Kelly et al. (2013b) used numerical modeling of diffusioncontrolled nucleation and growth to reproduce the crystal sizes and spatial distributions of minerals in 13 porphyroblastic rocks. They calculated ΔT = 5–67 °C and ΔG _{ r } = 0.7–5.8 kJ per mole of garnet. Spear et al. (2014) also evaluated the degree of disequilibrium for the garnetforming reaction. Using a combination of quartz in garnet barometry (QuiG) and thermodynamic modeling for garnet zone metamorphic rocks in eastern Vermont, they calculated a ΔT of 10 °C, a pressure overstep of 0.6 kbar, and a ΔG _{ r } of 2 kJ per mole of garnet. For the staurolite–kyanite zone in the same metamorphic terrain and for a blueschist sample from Sifnos, Greece, Spear et al. (2014) calculated a ΔT of 50 °C, a pressure overstep of 2–5 kbar, and a ΔG _{ r } of 10–18 kJ per mole of garnet. Although diverse methods have been used to infer the degree of disequilibrium for the garnetforming reaction, the calculated values suggest that in all cases the garnet nucleated and grew after a significant overstep from equilibrium conditions.
Wilbur and Ague (2006) used Monte Carlo simulations of crystal growth to demonstrate the formation of irregular and branching morphologies in garnet porphyroblasts. Because this simulation assumed random walk of chemical species, the morphology was produced by diffusioncontrolled growth. They determined that a minimum Gibbs free energy overstep of about 2 kJ per mole of garnet was needed to produce a branched morphology for silicate minerals (Wilbur and Ague 2006). This value is consistent with the Gibbs free energy overstep calculated in this paper. Spear and Daniel (2001) proposed an amoebalike growth model for garnet porphyroblasts based on observations of heterogeneous chemical zoning. This model supports the development of an irregular and branching morphology in garnet porphyroblasts. Collectively, the results obtained using these different approaches suggest that the irregular and branching morphology of garnet porphyroblasts is indicative of diffusioncontrolled growth.
Ostwald ripening and grain growth are not considered in this paper because the garnets occur as porphyroblasts, meaning that the size of the garnet crystals is much larger than the surrounding matrix minerals. Because grain growth associated with Ostwald ripening takes place due to the reduction of interfacial energy when the system is close to equilibrium, this mechanism should occur at a faster rate for smaller grain sizes. Hence, grain growth due to Ostwald ripening is only important for nonporphyroblastic minerals.
Figure 13 summarizes the relationships among supersaturation, temperature oversteps, and the critical grain diameter for diffusional instability with respect to the diffusioncontrolled growth of garnet porphyroblasts in the Tsukuba metamorphic rocks. It is clear that nucleation occurs after a significant overstep from equilibrium conditions for the garnetforming reaction. Figure 13 shows two different trends in garnet size vs. degree of supersaturation, with pathA and pathB representing nearly constant supersaturation and decreasing supersaturation during garnet growth, respectively. The supersaturation should decrease with consumption of the garnet component in the system. The rate of decrease of the garnet component depends on the relative magnitudes of the garnet precipitation rate and the dissolution rate of reactants in the garnetforming reaction. Both rates are limited by diffusion of the RLC. For simplicity, it was assumed that the garnet and reactant crystals are the same size.
If the number of garnet crystals is much fewer than the number of reactant crystals, the evolution of garnet size and degree of supersaturation should follow pathA. For diffusioncontrolled growth in this case, a small nucleation rate and large number of reactant crystals favor the growth of a small number of garnet crystals, thus producing unstable porphyroblastic garnet. Large garnet porphyroblasts with irregular and branching morphologies will form. Conversely, if the number of garnet crystals is much larger than the number of reactant crystals, the evolution of garnet size and degree of supersaturation should follow pathB. Due to a high nucleation rate and a small number of reactant crystals, many small garnets should grow rather than porphyroblasts. In addition, pathB promotes a stable garnet morphology, thus preventing the formation of branching and irregular textures.
Kelly et al. (2013b) proposed diffusioncontrolled growth for the formation of garnet porphyroblasts whereas Gaidies et al. (2011) proposed interfacecontrolled growth. Based on the mean radii of garnet porphyroblasts measured in these studies, the mean diameters of garnet porphyroblasts range from 180 to 2400 μm (Fig. 13). Most diameters fall in the range of 1000 to 2000 μm. Therefore, diffusioncontrolled growth of garnet porphyroblasts without the development of irregular and branching morphology is difficult to achieve. This finding contradicts the hypothesis that diffusioncontrolled growth of garnet porphyroblasts dominates in nature, which is consistent with the rarity of irregular and branching garnet porphyroblasts in metamorphic belts.
Over a scale of 10 cm, temperature heterogeneities produced by the growth of a garnet porphyroblast will be quickly dissipated over a time interval significantly shorter than the long growth period of the porphyroblast. This reasoning indicates that a control on porphyroblast growth by heat flow is unlikely. Therefore, the results of this study suggest that garnet porphyroblasts lacking an irregular and branching morphology (common in many metamorphic belts) may grow at a high degree of disequilibrium under interfacialcontrolled growth, provided they are set in a medium in which diffusion is rapid and the supply of elements from metamorphic fluids is sufficient.
Conclusions
Garnet porphyroblasts with an irregular morphology and a diffusional halo of reactants occur in the LP–HT Tsukuba metamorphic rocks of central Japan. The features observed suggest diffusioncontrolled growth of the porphyroblasts.
Using an analysis of diffusional instability, the degree of disequilibrium can be determined by measuring the dominant wavelength of the interface of the garnet porphyroblasts. The results show that the supersaturation is 0.05 × 10^{−1}–0.16. From the extent of supersaturation, the calculated overstep of Gibbs free energy from equilibrium is 0.9–27 kJ per mole of garnet (12 oxygen atoms), and the temperature overstep is 1.7–50 °C.
A high degree of disequilibrium for a garnetforming reaction is expected during growth of a garnet porphyroblast after nucleation. The present results suggest that garnet porphyroblasts that lack irregular and branching morphologies, a typical feature of many metamorphic belts, may grow at a high degree of disequilibrium under interfacialcontrolled growth, provided they are set in a medium where diffusion and the supply of elements is sufficient, such as a sufficient volume of metamorphic fluid.
Abbreviations
 FFT:

fast Fourier transform
 QuiG:

quartz in garnet barometry
 RLC:

ratelimiting component
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Acknowledgements
The author would like to express his gratitude to Dr. Tetsuo Kawakami and Kazuhiko Ishii who were conveners of the Japan Geoscience Union session on “Deformed Rocks, Metamorphic Rocks and Tectonics” for encouraging me to submit this paper to PEPS. I also thank two anonymous reviewers for their constructive reviews, comments, and suggestions that helped to improve the manuscript.
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Miyazaki, K. Diffusioncontrolled growth and degree of disequilibrium of garnet porphyroblasts: is diffusioncontrolled growth of porphyroblasts common?. Prog. in Earth and Planet. Sci. 2, 25 (2015). https://doi.org/10.1186/s4064501500554
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Keywords
 Diffusioncontrolled growth
 Garnet
 Metamorphism
 Disequilibrium
 Porphyroblast