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Statistical model selection between elastic and Newtonian viscous matrix models for the microboudin palaeopiezometer
Earth, Planets and Spacevolume 69, Article number: 83 (2017)
Abstract
We carried out statistical evaluations of two probability density functions for the microboudin palaeopiezometer using the Akaike information criterion (AIC) and the crossvalidation (CV) technique. In terms of the relevant stresstransfer model, these functions are defined as the elastic matrix model and the Newtonian viscous matrix model, respectively. The AIC and CV techniques enable us to evaluate the relative quality of both models when applied to nine data sets collected from metachert samples containing tourmaline grains in a quartz matrix, collected from the East Pilbara Terrane, Western Australia. The results show that the elastic matrix model is the more appropriate probability density function for analysis of fracturing of tourmaline grains in a quartz matrix. This statistical evaluation shows the validity of the elastic matrix model for the microboudin palaeopiezometer when analysing such data sets.
Introduction
Boudinage structure is a key to the stress and strain analysis of deformed rocks. Pioneering deformation analysis using this structure has been performed when measuring the strain of layered boudins (Ferguson 1981, 1985, 1987; Ferguson and Lloyd 1984; Lloyd and Condliffe 2003). These studies demonstrated a significant difference in magnitude between the stress generated within boudins and that experienced by the surrounding matrix (Lloyd et al. 1982). Ferguson and Lloyd (1982) challenged existing methods of estimating palaeostress and strain. These early studies inspired Masuda and coworkers to establish a palaeopiezometer using the microboudin structure of columnar grains (e.g. tourmaline, piemontite, and glaucophane) within quartzose or calcareous metamorphic tectonites (Masuda et al. 1989, 2003, 2008; Kimura et al. 2006, 2010).
The basis of the microboudin palaeopiezometer is the theoretical probability density function for the fracturing of columnar grains (Masuda et al. 1989, 2003). The function represents the relationship between the proportion of microboudinaged grains and the aspect ratio of analysed columnar grains. The proportion of microboudinaged grains is defined as the ratio of the number of boudinaged grains to the total number of grains (microboudinaged + intact) for each aspect ratio. The probability function representation is the most important aspect of the microboudin palaeopiezometer (e.g. Masuda et al. 2011). The validity of the analysis requires the identification of an appropriate probability density function for natural microboudin data (Masuda et al. 2008, 2011; Omori et al. 2016).
Masuda and Kimura (2004) assessed the applicability of two probability density functions, assuming a columnar mineral grain surrounded by an elastic matrix and a Newtonian viscous matrix, respectively. They suggested that this comparison favoured the assumption of an elastic matrix for the microboudin palaeopiezometer. However, Maeder et al. (2009) used finite element modelling of the development of segment structures, including boudins, to show that variation in boudinaged segment shape is dependent on the viscosity contrast between competent and incompetent layers, and the kinematic vorticity number. Komoróczi et al. (2013) also performed boudinage modelling that involved coupled deformation of brittle and viscous layers. Thus, a viscous matrix remains a general assumption when considering the development of boudinaged structures.
As the evaluation by Masuda and Kimura (2004) relied on a qualitative best fit for the data, their assessment is not definitive. This approach is neither satisfactory nor quantifiable. The assessment is unable to establish a distinct difference between the functions in the qualitative best fit for newly obtained data, and Masuda and Kimura’s (2004) approach fails to support the validity of using an elastic matrix for theoretical modelling of fracturing. To better establish the basis for the microboudin palaeopiezometer, quantitative evaluation is required to assess whether the assumption of an elastic matrix is valid and reliable for microboudinage structures.
In this study, therefore, we reexamined the applicability of the two probability density functions to natural microboudin data. A quantitative comparison of the two functions was achieved through statistical evaluation using the Akaike information criterion (AIC) and a crossvalidation (CV) technique. These statistical evaluations measure the relative quality of the models for a given data set, providing independent criteria to evaluate the fit of each probability density function (e.g. Burnham and Anderson 2002). Test data were obtained from columnar tourmaline grains containing microboudinaged structures, within metacherts collected from the Warrawoona greenstone belt in the East Pilbara Terrane, Western Australia.
Derivation of the probability density functions
Elastic matrix model
The fibreloading theory and the shearlag model, as applied to a columnar grain completely embedded within a continuous elastic matrix, assume that the matrix elastically transmits the farfield stress as a tensile stress along the grain (Fig. 1a). Using the shearlag model, Masuda et al. (2003) proposed that the probability density function could be expressed as an elastic matrix model \(G_{E} \left( {r;\lambda } \right)\) representing the relationship between the proportion of microboudinaged grains and the aspect ratio of columnar minerals. The function \(G_{E} \left( {r;\lambda } \right)\) was referred to as \(G\left( {r;\lambda } \right)\) in previous theoretical works on the microboudin palaeopiezometer (Masuda et al. 2003, 2011; Kimura et al. 2006, 2010). In this paper, however, we represent the function as \(G_{E} \left( {r;\lambda } \right)\) to allow comparison with the Newtonian viscous matrix model. \(G_{E} \left( {r;\lambda } \right)\) is a function of the aspect ratio of columnar grains r and a nondimensional stress parameter λ as follows (Masuda et al. 2003; Kimura et al. 2010):
where m is the Weibull parameter; E _{ f } and E _{ q } are the elastic constants of the columnar grains and the matrix, respectively; and A _{0} is a constant (Masuda et al. 2003). In the present study of tourmaline grains within a quartz matrix, the constants \({{E_{f} } \mathord{\left/ {\vphantom {{E_{f} } {E_{q} }}} \right. \kern0pt} {E_{q} }}\) and A _{0} have values of 2 and 0.4, respectively (Kimura et al. 2010). The relationship between λ and farfield differential stress σ _{0} was defined by Kimura et al. (2010) as follows:
where \(S_{0}^{**}\) is the instantaneous modal fracture strength of a 1mm cube of a columnar mineral grain, K _{ c } is the fracture toughness, K _{0} is the subcritical crack growth limit, and \(\overline{w}\) is the geometric mean width of the grains. This equation considers the influence of time (Masuda et al. 2008) and the effect of size on fracture strength for columnar grains (Kimura et al. 2010). Among the parameters in Eq. (2), Kimura et al. (2006, 2010) determined that \(S_{0}^{**}\) = 39, 64, and 80 MPa for tourmaline, epidote, and amphibole, respectively. Moreover, Masuda et al. (2008) tentatively proposed that \({{K_{0} } \mathord{\left/ {\vphantom {{K_{0} } {K_{c} }}} \right. \kern0pt} {K_{c} }}\) = 0.1. The microboudin palaeopiezometer combines the above equations to estimate σ _{0} (e.g. Masuda et al. 2008, 2011).
Newtonian viscous matrix model
Ramberg (1955) solved the stress and strain parameters in a competent layer subjected to onedimensional elongation as a function of the strain rate of the surrounding Newtonian viscous matrix (Fig. 1b). Drag forces acting on the Newtonian viscous matrix in the competent layer cause fracturing when the matrix flows along the layer. Based on the Ramberg (1955) solution, Masuda and Kimura (2004) proposed that the fracturing of columnar grains is equivalent to the competent layer described by the Newtonian viscous model \(G_{V} \left( {r;\psi } \right)\). \(G_{V} \left( {r;\psi } \right)\) is a function of the aspect ratio r and a dimensionless parameter ψ as follows:
and ψ is defined as
As the Weibull parameter depends on the fracture strength of columnar grains, we use m = 2 in the case for the elastic model. The terms z _{ C } and z _{ i } in Eq. (4) are the thicknesses of the competent layer and matrix, respectively; σ _{0} is the farfield differential stress; and S* is the fracture strength of competent material at r = 1, which is regarded as a materialdependent constant (Masuda and Kimura 2004). In the Newtonian viscous model, farfield differential stress (σ _{0}) is defined as:
where μ is the matrix viscosity and \({{  \partial \left( {{z \mathord{\left/ {\vphantom {z {z_{i} }}} \right. \kern0pt} {z_{i} }}} \right)} \mathord{\left/ {\vphantom {{  \partial \left( {{z \mathord{\left/ {\vphantom {z {z_{i} }}} \right. \kern0pt} {z_{i} }}} \right)} {\partial t}}} \right. \kern0pt} {\partial t}}\) is the compressional strain rate along the z axis.
Basic data sets for model evaluation
Our statistical approach requires data to evaluate the elastic matrix and Newtonian viscous matrix models. The data we apply here are the proportion of microboudinaged columnar grains with respect to their aspect ratio (p _{ r }), defined as the ratio of the number of microboudinaged grains to the total number of grains (microboudinaged + intact) for each aspect ratio. Such data can be obtained by measuring columnar mineral grains in samples of metamorphic tectonites. In this study, we obtained nine data sets from tourmaline grains embedded within the quartz matrix of metacherts collected from the Warrawoona Greenstone Belt around the Mount Edgar and Corunna Downs granitoid complexes in the East Pilbara Terrane (Fig. 2). It has been reported that greenstones in this area underwent greenschistfacies metamorphism, except near the margins of the associated granitoid domes, where conditions locally reach amphibolite facies as a probable result of contact metamorphism (e.g. Delor et al. 1991; Collins and Van Kranendonk 1999). The geological setting and detailed observations of this region have been provided by Collins et al. (1998, 1999) and Van Kranendonk et al. (2002, 2004, 2007). The nature of the metachert samples and the corresponding data sets are briefly described below.
Analysed samples
The samples are composed mainly of equigranular quartz (grain size = tens of µm to > 0.1 mm), together with tourmaline, chlorite, and muscovite. A consistent foliation is present, defined by the alignment of muscovite and quartzrich layers of contrasting colours. A prominent mineral lineation is also defined within these rocks by the alignment of the long axes of tourmaline on this foliation surface, as measured using the method of Masuda et al. (1999) (Fig. 3).
Microboudinage structure of tourmaline grains
Some tourmaline grains show a microboudinage structure within the quartz matrix (Fig. 4). The microboudinaged tourmaline grains have the following characteristics: (1) they are fractured perpendicular to their long axes; (2) they are generally pulled apart without any evidence of significant rotation during separation; and (3) the interboudin gaps are filled with quartz. These observations suggest that the morphological characteristics of the microboudinaged tourmaline grains are of the unmodified symmetric type, torn boudins group, and block (object) boudins according to the classification scheme of Goscombe et al. (2004).
Proportion of microboudinage
We collected nine data sets from tourmaline grains on the foliation surface according to the procedure of Masuda et al. (2011). We measured the widths and lengths of tourmaline grains and the distances of the interboudin gaps in microboudinaged tourmaline grains on foliation surfaces, for grains with long axes oriented within 15° of the mineral lineation (Fig. 5). The basic data for the model evaluation consist of the proportion of microboudinaged grains with respect to the aspect ratio (r). The frequency distributions of microboudinaged and intact columnar grains are shown in Fig. 6, and the proportions of microboudinaged grains are plotted in Fig. 7.
Model evaluation
The AIC and CV techniques were used to calculate the value of AIC and the generalization error for the elastic and Newtonian viscous matrix models for each data set. Given that both values reflect the relative predictive performance of the models when using unknown data (e.g. Burnham and Anderson 2002; Bishop 2006), we use these values as an indicator of the relative quality of the two models. We briefly explain both approaches below.
AIC
AIC is a powerful model testing criterion proposed by Akaike (1974) that has been widely used for model selection in various scientific fields (e.g. Sclove 1987; Hansen 1999; Mazerolle 2006; Ahmed et al. 2007; Posada 2008). AIC is mathematically based on the Kullback–Leibler information of distance (e.g. Kullback and Leibler 1951), which is a way of measuring differences among probability distributions. Akaike (1974) developed a rigorous method to estimate the Kullback–Leibler information based on the empirical loglikelihood function at its maximum point as the AIC (Burnham and Anderson 2002, 2004) as follows:
where L _{max} is the maximum likelihood and M is the number of independently adjusted parameters. The preferred model is that with the minimum AIC value. The AIC value is used here to identify either the elastic or Newtonian model as the more appropriate. The value of M in both models is 1, which is the stress parameter λ or ψ in the elastic and Newtonian models, respectively. L _{max} is the fundamental value used to evaluate the models by AIC, and this can be obtained from the maximum likelihood estimation.
In maximum likelihood estimation, we adopted the binomial distribution (e.g. Savage 1972) as the error function of the data at each measurement point, which consists of the proportion of microboudinaged columnar grains as a function of the aspect ratio, because columnar mineral grains are divided into two classes according to whether they are microboudinaged.
The binomial distribution is a discrete probability distribution with parameters N and p as follows:
where
In probability theory and statistics, N is the number of successes in a sequence of yesorno experiments, y is the number of success (y = 0, 1, 2,…, N), and p is the probability of success. Given that we treat a success as being a fractured grain, then for the microboudinage data set N is the total number of measured grains, y is the number of microboudinaged grains, and p is the ratio of the number of microboudinaged grains to the total number of grains (microboudinaged + intact). In the microboudinage case, the value of p _{ r } is represented in the elastic matrix and Newtonian viscous matrix models as follows:
and
respectively. The likelihood functions L _{ E } and L _{ V } are defined by the infinite product of Eq. (7) for the elastic and Newtonian viscous matrix models in Eqs. (9) and (10) as follows:
and
respectively. \(N_{{r_{i} }}\) and \(y_{{r_{i} }}\) are N and y for the measurement point i, respectively.
We then evaluated the stress parameters λ and ψ using maximum likelihood estimation (e.g. Savage 1972). This approach provides the value of maximum likelihood L _{max} for Eqs. (11) and (12), along with the corresponding stress parameters (λ and ψ) used to solve the optimization problem.
Crossvalidation
AIC provides a useful solution for selecting the best model. However, if the available data are poor, then the best model selected might still be poor (Burnham and Anderson 2004). Thus, every effort must be made to ensure that the data used are high quality, and we acknowledge the limitation of our data in this respect. This problem commonly arises in deformation analysis of metamorphic tectonites. To rigorously evaluate the relative quality of the models, it may be necessary to obtain a test data set on which the performance of the selected model is finally evaluated.
As such, we used the CV technique to address this problem. The CV technique is an effective method for evaluating the predictive capability of a statistical model for an unknown data set based on the generalization error (GE) (e.g. Bishop 2006; Kuwatani et al. 2014), and this approach has been generally applied to model selection (e.g. Stone 1974, 1977; Geisser 1975). In the CV technique, the given data set is divided into training and testing subsets. We used the training subset to construct a statistical model and then used the test subset to evaluate the predictive performance of the model. In effect, we regard a part of the data sets as unknown data and then evaluate the predictive performance of the model for the unknown data.
In this study, we adopted the leaveoneout (LOO) method for the CV. The LOO method divides the data set into N (the number of data points) parts and then uses \({{\left( {N  1} \right)} \mathord{\left/ {\vphantom {{\left( {N  1} \right)} N}} \right. \kern0pt} N}\) parts of the data as the training subset z _{ i } and the remaining part of the data as the test subset x _{ i } for the CV. This procedure is then repeated for all N possible choices (Bishop 2006). In this study, the LOO method was adopted to calculate the GE _{ E } and GE _{ V }, corresponding to the probability density functions \(G_{E} \left( {r;\lambda } \right)\) and \(G_{V} \left( {r;\psi } \right)\) as follows:
and
respectively, where n is the number of data points, and \(E\left( {x_{i} ,G_{E} \left( {z_{i} ;\lambda_{i} } \right)} \right)\) and \(E\left( {x_{i} ,G_{V} \left( {z_{i} ;\psi_{i} } \right)} \right)\) are the error of the testing subsets x _{ i } corresponding to the probability distributions of the constructed models \(G_{E} \left( {r;\lambda } \right)\) and \(G_{V} \left( {r;\psi } \right)\), respectively. The set of statistical parameters λ _{ i } and ψ _{ i } was determined using the training subset z _{ i } that consists of all the data, apart from the testing subset x _{ i }. When using the maximum likelihood approach, the error functions \(E\left( {x_{i} ,G_{E} \left( {z_{i} ;\lambda_{i} } \right)} \right)\) and \(E\left( {x_{i} ,G_{V} \left( {z_{i} ;\psi_{i} } \right)} \right)\) are represented as:
and
respectively. \(N_{i}^{{\left( {x_{i} } \right)}}\) is the total number of measured grains in the testing subset and x _{ i }, \(y_{i}^{{\left( {x_{i} } \right)}}\) is the number of microboudinaged grains in the testing subset x _{ i }. Equations (15) and (16) provide the function of likelihood given by the testing subset x _{ i } in each model. The model that has a smaller generalization error value is determined to be the better model, based on its higher predictive performance for the unknown data.
Results
The values of AIC, GE _{ E }, and GE _{ V } can be calculated from Eqs. (6), (13), and (14), respectively. We determined these values for both models using the nine data sets. Figure 6 shows the frequency distribution of microboudinaged tourmaline grains, which is characterized as the number of microboudinaged (grey bar) and intact grains (white bar) for each aspect ratio bin. Based on the maximum likelihood estimation applied to the data displayed in Fig. 6, we obtained the p _{ r } values and bestfit curves for \(G_{E} \left( {r;\lambda } \right)\) and \(G_{V} \left( {r;\psi } \right)\), and the values of λ and ψ for each data set (Fig. 7). These curves show that the values of p _{ r } continuously increase with increasing aspect ratio of the tourmaline grains. The 95% confidence interval of each p _{ r } value represents the proportion of data from grains with a much larger aspect ratio (r > 10) that have lower quality than the grains with a smaller aspect ratio (r < 5), because the total number of grains is small (i.e. <25 grains, as shown in Fig. 6).
According to the values of AIC, GE _{ E }, and GE _{ V }, these criteria show that the elastic model always has smaller values than the Newtonian viscous matrix model. Thus, these statistical constraints identify the elastic matrix model as the appropriate model for the fracturing of tourmaline grains in all the analysed samples (Table 1). From the perspective of the goodness of fit, the data from sample EP6fb clearly show a much better fit to the elastic matrix model than the Newtonian viscous model, whereas for the other eight samples there are no significant differences between the models. This result indicates that a qualitative assessment (e.g. Masuda and Kimura 2004 ) does not always successfully identify the appropriate model for a given data set. Values of p _{ r } for grains with a high aspect ratio (r > 10) are significantly larger than predicted by \(G_{E} \left( {r;\lambda } \right)\). These data ostensibly match \(G_{V} \left( {r;\psi } \right)\) (Fig. 7), although they are insignificant in determining the quality of the model. Given that both models have only one parameter, the AIC evaluation is essentially the same as that derived from maximum loglikelihood values.
Statistical criteria can be used to objectively assess the validity of the elastic matrix model applied to the microboudin palaeopiezometer. A substantial advantage of using information criteria such as AIC is that they are applicable to nonnested models (Burnham and Anderson 2002). In such models, one proposed model cannot be a subset of other models, as is the case for the elastic matrix and Newtonian viscous matrix models compared here. However, the information criteria must be chosen carefully for nonnested models due to the large possible variance in AIC (e.g. Ripley 2004). For the data sets examined in this study, AIC values for the elastic matrix model are approximately half of those for the Newtonian viscous matrix model (Table 1). These differences indicate that it is reasonable to regard the elastic matrix model as suitable for the microboudin palaeopiezometer for the analysed data sets.
Discussion
Evaluation of the results
Our result showed the validity of the elastic matrix model using for the microboudin palaeopiezometer and quantitatively supported the conclusion in Masuda and Kimura (2004); as the microboudinage occurred in the solid state during metamorphism, the elastic matrix model is acceptable. However, we do not conclude that the elastic matrix model is the best model for all microboudin data. The criteria used in this study were selected to enable comparison between the relative predictive performance of the elastic and Newtonian viscous models for nine data sets, and there are no threshold AIC or GE values that indicate the need to discard or adapt the models. It is possible that an alternative model, such as a nonNewtonian viscous model, would be more suitable than the elastic matrix model, although no other models have been proposed for the microboudin palaeopiezometer. The statistical modelselection approach could be used to undertake an objective comparison between the elastic matrix model and an alternative.
Significance of the elastic model
As the fracturing of columnar grains occurs under solidstate flow during metamorphism (e.g. Masuda et al. 2011), it is reasonable to use the elastic model to simulate the fracturing of columnar grains. Microboudinage of columnar grains into two segments can be considered to occur via the following three stages (Ferguson 1981; Lloyd et al. 1982; Masuda and Kuriyama 1988): (1) prefracturing; (2) fracturing; and (3) separation. The probability density function considers stages (1) and (2) and describes the proportion of microboudinaged grains as a function of aspect ratio (Fig. 7). By focussing on the duration of the fracturing and separation stages, we consider the applicability of the elastic matrix model to microboudinage.
There is a significant difference in the duration of the fracturing and separation of columnar grains. Fracturing of a columnar grain is generally assumed to occur instantaneously when the applied stress reaches the fracture strength of a microcrack within the grain (e.g. Masuda et al. 1989, 2003). However, according to the principles of fracture mechanics (e.g. Davidge 1979; Atkinson 1987; Lawn 1993; Anderson 2005; Gdoutos 2005), crack growth proceeds gradually at stresses lower than the fracture strength and results in a process with a relatively slow crack velocity, known as subcritical crack growth (e.g. Masuda et al. 2008). The slowest crack velocity estimated to date is 5 × 10^{−12} m/s (Wilkins 1980), with 1mmlong cracks being produced in only 10^{2} years. As fracturing occurs at a critical crack length, which is <50 μm in the analysed tourmaline grains, the observed fractures can form in several decades. Compared with ductile flow during metamorphism that occurs on the geological timescale (i.e. at least 10^{6} years; e.g. Brown 2010; Hobbs and Ord 2014), cracks propagate instantaneously through intact grains to generate fractures even if the fracturing proceeded with an extremely slow crack velocity (Masuda et al. 2008).
During the separation stage, the shape of boudinaged segments is often determined by ductile deformation associated with viscous flow of the surrounding matrix (e.g. Malavieille and Lacassin 1988; Goscombe et al. 2004; Maeder et al. 2009). Previous simulations have successfully reproduced the various observed shapes of boudinaged segments (e.g. Lloyd and Ferguson 1981; Treagus and Lan 2004; Maeder et al. 2009; Komoróczi et al. 2013). Therefore, fracturing of columnar grains can be reasonably simulated under the assumption of an elastic matrix, whereas the variation in segment shape requires a ductile matrix. This discrepancy may be due to the significant difference in timescales of duration between fracturing (~10^{2} years) and separation (~10^{6} years). This difference suggests that the elastic and viscous matrix models can be compatible in terms of the development of microboudinage structures during metamorphism. However, the limitation of this compatibility remains problematic, although viscous theory has been applied to solidstate flow in the crust (e.g. MacKenzie 1979; Weijermars 1986; Masuda and Ando 1988; Passchier and Sokoutis 1993; Arbaret et al. 2001; Jiang 2007, 2012; Mancktelow et al. 2002; Mancktelow 2013). The technique of statistical model evaluation is a valuable approach with which to address this problem.
Conclusions
We statistically evaluated the suitability of probability density functions describing elastic and Newtonian viscous matrix models via AIC and the CV technique, using natural data from the microboudinage structure of tourmaline grains within a quartz matrix contained within metacherts. Our statistical evaluation revealed that the elastic matrix model is the more appropriate probability density function for the fracturing of columnar grains. This result supports the use of the elastic matrix model for palaeostress analysis by the microboudin palaeopiezometer. The microboudinage structure of columnar grains is one of the forms of evidence commonly used to estimate the palaeostress state imposed on metamorphic tectonites. Constructing a theoretical model for microboudinage and evaluating the model is essential to constraining geodynamics through such deformation analysis. We encourage further tests of the theoretical model for the microboudin palaeopiezometer and suggest that the statistical approach outlined here will offer an important contribution to validating such future developments in the application of stress analysis to metamorphic tectonites.
Abbreviations
 AIC:

Akaike information criterion
 CV:

crossvalidation
 LOO:

leaveoneout
References
Ahmed A, Sharma ML, Sharma A (2007) Wavelet based automatic phase picking algorithm for 3component broadband seismological data. J Seismol Earthq Eng 9:15
Akaike H (1974) A new look at the statistical model identification. IEEE Autom Control 19:716–723
Anderson TL (2005) Fracture mechanics: fundamentals and applications. CRC Press, Boca Raton
Arbaret L, Mancktelow N, Burg JP (2001) Effect of shape and orientation on rigid particle orientation and matrix deformation in simple shear flow. J Struct Geol 23:113–125
Atkinson BK (1987) Fracture mechanics of rock. Academic Press, London
Bishop CM (2006) Pattern recognition and machine learning. Springer, New York
Brown M (2010) The spatial and temporal patterning of the deep crust and implications for the process of melt extraction. Philos Trans R Soc A 368(1910):11–51
Burnham KP, Anderson DR (2002) Model selection and multimodel inference: a practical informationtheoretic approach. Springer, New York
Burnham KP, Anderson DR (2004) Multimodel inference understanding AIC and BIC in model selection. Sociol Methods Res 33:261–304
Collins WJ, Van Kranendonk MJ (1999) Model for the development of kyanite during partial convective overturn of Archean granite–greenstone terranes: the Pilbara Craton, Australia. J Metamorph Geol 17:145–156
Collins WJ, Van Kranendonk MJ, Teyssier C (1998) Partial convective overturn of Archaean crust in the east Pilbara Craton, Western Australia: driving mechanisms and tectonic implications. J Struct Geol 20:1405–1424
Davidge RW (1979) Mechanical behaviour of ceramics. Cambridge University Press, London
Delor C, Burg JP, Clarke G (1991) Relations diapirismemétamorphisme dans la Province du Pilbara (Australie Occidentale): implications pour les régimes thermiques et tectoniques à l'Archéen. Comptes rendus de l'Académie des sciences. Série 2, Mécanique, Physique, Chimie, Sciences de l'univers, Sciences de la Terre 312:257–263
Ferguson CC (1981) A strain reversal method for estimating extension from fragmented rigid inclusions. Tectonophysics 73:43–52
Ferguson CC (1985) Spatial analysis of extension fracture systems: a process modelling approach. J Int Assoc Math Geol 17:403–425
Ferguson CC (1987) Fracture and separation histories of stretched belemnites and other rigidbrittle inclusions in tectonites. Tectonophysics 139:255–273
Ferguson CC, Lloyd GE (1982) Palaeostress and strain estimates from boudinage structure and their bearing on the evolution of a major Variscan foldthrust complex in Southwest England. Tectonophysics 88:269–289
Ferguson CC, Lloyd GE (1984) Extension analysis of stretched belemnites: a comparison of methods. Tectonophysics 101:199–206
François C, Philippot P, Rey P, Rubatto D (2014) Burial and exhumation during Archean subduction in the East Pilbara granite–greenstone terrane. Earth Planet Sci Lett 396:235–251
Gdoutos EE (2005) Fracture mechanics: an introduction, 2nd edn. (vol. 123 of solid mechanics and its applications)
Geisser S (1975) The predictive sample reuse method with applications. J Am Stat Assoc 70:320–328
Goscombe BD, Passchier CW, Martin H (2004) Boudinage classification: endmember boudin types and modified boudin structures. J Struct Geol 26:739–763
Hansen JW (1999) Stochastic daily solar irradiance for biological modeling applications. Agric For Meteorol 94(1):53–63
Hobbs BE, Ord A (2014) Structural geology: the mechanics of deforming metamorphic rocks. Elsevier, Amsterdam
Jiang D (2007) Numerical modeling of the motion of rigid ellipsoidal objects in slow viscous flows: a new approach. J Struct Geol 29(2):189–200
Jiang D (2012) A general approach for modeling the motion of rigid and deformable ellipsoids in ductile flows. Comput Geosci 38(1):52–61
Kimura N, Awaji H, Okamoto M, Matsumura Y, Masuda T (2006) Fracture strength of tourmaline and epidote by threepoint bending test: application to microboudin method for estimating absolute magnitude of palaeodifferential stress. J Struct Geol 28:1093–1102
Kimura N, Nakayama S, Tsukimura K, Miwa M, Okamoto A, Masuda T (2010) Determination of amphibole fracture strength for quantitative palaeostress analysis using microboudinage structure. J Struct Geol 32:136–150
Kloppenburg A, White SH, Zegers TE (2001) Structural evolution of the Warrawoona Greenstone Belt and adjoining granitoid complexes, Pilbara Craton, Australia: implications for Archaean tectonic processes. Precambrian Res 112(1):107–147
Komoróczi A, Abe S, Urai JL (2013) Meshless numerical modeling of brittleviscous deformation: first results on boudinage and hydrofracturing using a coupling of discrete element method (DEM) and smoothed particle hydrodynamics (SPH). Comput Geosci 17:373–390
Kullback S, Leibler RA (1951) On information and sufficiency. Ann Math Stat 22:79–86
Kuwatani T, Nagata K, Okada M, Watanabe T, Ogawa Y, Komai T, Tsuchiya N (2014) Machinelearning techniques for geochemical discrimination of 2011 Tohoku tsunami deposits. Sci Rep 4:7077. doi:10.1038/srep07077
Lawn B (1993) Fracture of brittle solids, 2nd edn. Cambridge University Press, Cambridge
Lloyd GE, Condliffe E (2003) ‘Strain Reversal’: a Windows™ program to determine extensional strain from rigidbrittle layers of inclusions. J Struct Geol 25:1141–1145
Lloyd GE, Ferguson CC (1981) Boudinage structure: some new interpretations based on elasticplastic finite element simulations. J Struct Geol 3(2):117–128
Lloyd GE, Ferguson CC, Reading K (1982) A stresstransfer model for the development of extension fracture boudinage. J Struct Geol 4:355–372
MacKenzie D (1979) Finite deformation during fluid flow. Geophys J Int 58:687–715
Maeder X, Passchier CW, Koehn D (2009) Modelling of segment structures: boudins, boneboudins, mullions and related singleand multiphase deformation features. J Struct Geol 31:817–830
Malavieille J, Lacassin R (1988) ‘Boneshaped’boudins in progressive shearing. J Struct Geol 10:335–345
Mancktelow NS (2013) Behaviour of an isolated rimmed elliptical inclusion in 2D slow incompressible viscous flow. J Struct Geol 46:235–254
Mancktelow N, Arbaret L, Pennacchioni G (2002) Experimental observations on the effect of interface slip on rotation and stabilisation of rigid particles in simple shear and a comparison with natural mylonites. J Struct Geol 24:567–585
Masuda T, Ando S (1988) Viscous flow around a rigid spherical body: a hydrodynamical approach. Tectonophysics 148:337–346
Masuda T, Kimura N (2004) Can a Newtonian viscousmatrix model be applied to microboudinage of columnar grains in quartzose tectonites? J Struct Geol 26:1749–1754
Masuda T, Kuriyama M (1988) Successive “midpoint” fracturing during microboudinage: an estimate of the stress–strain relation during a natural deformation. Tectonophysics 147:171–177
Masuda T, Shibutani T, Igarashi T, Kuriyama M (1989) Microboudin structure of piemontite in quartz schists: a proposal for a new indicator of relative palaeodifferential stress. Tectonophysics 163:169–180
Masuda T, Kugimiya Y, Aoshima I, Hara Y, Ikei H (1999) A statistical approach to determination of a mineral lineation. J Struct Geol 21:467–472
Masuda T, Kimura N, Hara Y (2003) Progress in microboudin method for palaeostress analysis of metamorphic tectonites: application of mathematically refined expression. Tectonophysics 364:1–8
Masuda T, Nakayama S, Kimura N, Okamoto A (2008) Magnitude of σ_{1}, σ_{2} and σ_{3} at midcrustal levels in an orogenic belt: microboudin method applied to an impure metachert from Turkey. Tectonophysics 460:230–236
Masuda T, Miyake T, Kimura N, Okamoto A (2011) Application of the microboudin method to palaeodifferential stress analysis of deformed impure marbles from Syros, Greece: implications for grainsize and calcitetwin palaeopiezometers. J Struct Geol 33:20–31
Mazerolle MJ (2006) Improving data analysis in herpetology: using Akaike’s information criterion (AIC) to assess the strength of biological hypotheses. AmphibReptil 27:169–180
Omori Y, Barresi A, Kimura N, Okamoto A, Masuda T (2016) Contrast in stressstrain history during exhumation between highand ultrahighpressure metamorphic units in the Western Alps: microboudinage analysis of piemontite in metacherts. J Struct Geol 89:168–180
Passchier CW, Sokoutis D (1993) Experimental modelling of mantled porphyroclasts. J Struct Geol 15:895–909
Posada D (2008) jModelTest: phylogenetic model averaging. Mol Biol Evol 25:1253–1256
Ramberg H (1955) Natural and experimental boudinage and pinchandswell structures. J Geol 63:512–526
Ripley BD (2004) Selecting amongst large classes of models. Methods and models in statistics: In honor of Professor John Nelder, FRS, pp 155–170
Savage LJ (1972) The foundations of statistics. Courier Corporation, New York
Sclove SL (1987) Application of modelselection criteria to some problems in multivariate analysis. Psychometrika 52:333–343
Stone M (1974) Crossvalidatory choice and assessment of statistical predictions. J R Stat Soc Ser B Methodol 36:111–147
Stone M (1977) An asymptotic equivalence of choice of model by crossvalidation and Akaike’s criterion. J R Stat Soc Ser B Methodol 39:44–47
Thébaud N, Rey PF (2013) Archean gravitydriven tectonics on hot and flooded continents: controls on longlived mineralised hydrothermal systems away from continental margins. Precambrian Res 229:93–104
Treagus SH, Lan L (2004) Deformation of square objects and boudins. J Struct Geol 26:1361–1376
Van Kranendonk MJ, Hickman AH, Smithies RH, Nelson DR (2002) Geology and tectonic evolution of the archean North Pilbara Terrane, Pilbara Craton, Western Australia. Econ Geol 97:695–732
Van Kranendonk MJ, Collins WJ, Hickman AH, Pawley MJ (2004) Critical tests of vertical vs. horizontal tectonic models for the Archaean East Pilbara Granite–Greenstone Terrane, Pilbara Craton, Western Australia. Precambrian Res 131:173–211
Van Kranendonk MJ, Smithies RH, Hickman AH, Champion DC (2007) Review: secular tectonic evolution of Archean continental crust: interplay between horizontal and vertical processes in the formation of the Pilbara Craton, Australia. Terra Nova 19:1–38
Weijermars R (1986) Flow behaviour and physical chemistry of bouncing putties and related polymers in view of tectonic laboratory applications. Tectonophysics 124:325–358
Wilkins BJS (1980) Slow crack growth and delayed failure of granite. Int J Rock Mech Min Sci Geomech Abst 17:365–368
Zhao P, Ji S (1997) Refinements of shearlag model and its applications. Tectonophysics 279:37–53
Authors’ contributions
TM drafted the manuscript, analysed data, and prepared the figures. TK and TM assisted in drafting the manuscript and participated in discussion. All authors read and approved the final manuscript.
Acknowledgements
We thank Toru Takeshita for his kind handling of our manuscript and two anonymous reviewers for their careful reviews and constructive comments. This study was supported by the Cooperative Research Program of the Earthquake Research Institute, University of Tokyo. The authors are grateful to Hideki Mori for preparing thin sections. The authors also thank G. E. Lloyd for constructive comments that helped to improve the manuscript. This work was financially supported in part by the JST PRESTO (Grant Number JPMJPR1676) and the Japan Society for the Promotion of Science (JSPS) KAKENHI Nos. 25120005, 25280090, and 15K20864, and the Japan Science and Technology Agency (JST), PRESTO No. 960323.
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Keywords
 Microboudinage structure
 AIC
 Crossvalidation
 Statistical model selection
 Elastic matrix model
 Newtonian viscous matrix model