Geological Objects and Physical Parameter Fields in the Subsurface: A Review

  • Guillaume Caumon
Open Access


Geologists and geophysicists often approach the study of the Earth using different and complementary perspectives. To simplify, geologists like to define and study objects and make hypotheses about their origin, whereas geophysicists often see the earth as a large, mostly unknown multivariate parameter field controlling complex physical processes. This chapter discusses some strategies to combine both approaches. In particular, I review some practical and theoretical frameworks associating petrophysical heterogeneities to the geometry and the history of geological objects. These frameworks open interesting perspectives to define prior parameter space in geophysical inverse problems, which can be consequential in under-constrained cases.

28.1 Introduction

The earth is three-dimensional, heterogeneous and, for its major part, inaccessible to direct observations. A consequence is that the static and dynamic parameters governing physical processes below the earth surface are generally poorly known. A recurrent challenge for geoscientists and engineers is, therefore, to predict the likely nature or behavior of the subsurface from limited data. In all fields of geophysics sensu lato, these forecasts may use physically and mathematically-based data processing (such as upward continuation of potential fields, seismic processing, classical processing of ground penetrating radar (Nobakht et al. 2013), reservoir production decline curves (Davis and Annan 1989; Fetkovich 1980, Fig. 28.1a), or the resolution of an inverse problem that explicitly uses physical models computing observations from some earth parameters and physical parameters (Fig. 28.1b–d, f–h). In geology, forecasts (e.g., about the location and volume of a specific formation or resource) and geological scenarios involve direct observations and geophysical images (Jackson and Rotevatn 2013; Perrouty et al. 2014; Fig. 28.1e). In this process, the loop may not always close: in the end, the interpretations are not guaranteed to be compatible with the initial geophysical observations. This may or may not be a problem, depending on the purpose of this interpretation. For example, a qualitative match between reflection seismic data and structural interpretations is probably sufficient to discuss fault growth models (Jackson and Rotevatn 2013), whereas such mismatch can be problematic in other tasks such as natural resource assessment (Caumon 2010; Jessell et al. 2014). Another practical problem is the interpretation and fusion of several independent data sets corresponding to different physical or geological observations (Corbel and Wellmann 2015; Paasche 2016). Geostatistics (Chiles and Delfiner 2012; Goovaerts 1997) was historically developed with these problems in mind, and is an attractive theoretical framework to recombine point and volume data coming from geophysical images consistently with spatial statistics. However geological reasoning and statistical reasoning are of different nature (Frodeman 1995), so honoring some spatial statistics is very useful but not always sufficient to represent geological concepts. Therefore, several methodologies have been introduced to explicitly incorporate geological knowledge in subsurface interpretation, all of them explicitly considering geological objects (Fig. 28.1f–h).
Fig. 28.1

Examples of approaches and workflows using geological and geophysical data to make forecasts about the earth or the associated processes and some illustrative references. a-d workflows that use no or minimal geological prior information. e classical use of geophysical data in fundamental and applied geology. f-h workflows that explicitly incorporate geological parameters in the process

The main focus of this chapter is to review the main frameworks by which geological concepts can be represented in earth models and inverse methods addressing several types of physics. Thus, it aims at complementing the existing reviews and discussions of Linde et al. (2015) and Jessell et al. (2014), who address this problem with similar objectives but different perspectives. As the topic is very vast, the reader is also referred to previous review papers related to this topic (Farmer 2005; Lelièvre and Farquharson 2016; Linde et al. 2015; de Marsily et al. 2005; Mosegaard and Hansen 2016; Oliver and Chen 2011; Pyrcz et al. 2015; Zhou et al. 2014a). Several books also present complementary perspectives and more complete descriptions and details (Agterberg 2014; Caers 2011; Mallet 2002, 2014; Perrin and Rainaud 2013; Pyrcz and Deutsch 2014). Section 28.2 provides further motivations for considering geology in geophysical models, and tries to define what “geology” means in that sense. Then, Sect. 28.3 briefly describes the type of parameterizations classically used in computational physics. We discuss some links between these physical parameterizations and the frameworks used to represent geological domains in Sect. 28.4.

28.2 Motivations for Explicit Geological Parameterizations

A wealth of perspectives is essential and complementary to make progresses in the understanding of our planet and its resources. This is exemplified by the various disciplines involved in natural resource characterization, see for instance Ringrose and Bentley (2015). Feedbacks and interactions between the various approaches generate many types of possible workflows to integrate geological data and produce forecasts, as illustrated in Fig. 28.1. For example, geophysical processing and inverse methods that use minimal geological prior information (Fig. 28.1a–d) are typically considered as data for geological interpretations (Fig. 28.1e). Whereas these “minimal prior” approaches are not this chapter’s focus, they are very useful and are always used to some extent in practical studies, because they provide at least a useful first-order view of the geological domain. This is illustrated in particular in deterministic workflows of Fig. 28.1h that strive for fit-for purpose, simplest as possible, subsurface models (Elrafie et al. 2008; Ringrose and Bentley 2015; Williams et al. 2004). They are also conceptually satisfying in the sense that they produce images or forecasts that mainly depend on the physics, hence can be claimed to be parsimonious and objective. As a consequence of this parsimony and of the non-linear nature of most involved physical processes, these models make it difficult to evaluate uncertainty (Watson et al. 2013). The term “objective” is also relative, as some choices are always made in these methods. In data processing methods these subjective choices relate to the underlying model assumptions (e.g., sub-horizontal layers). In inverse methods, choices must also be made about the parameterization, and a statistical model (e.g., the multi-Gaussian model) or a particular regularization (e.g., Mosegaard 2011).

Among the approaches that try to get the most out of the physics with minimal assumptions, recent and most promising developments use several types of data and petrophysical models to constrain local anisotropy, (see for instance Clapp et al. 2004; Ma et al. 2012; Sava et al. 2014; Zhou et al. 2014b) and recent reviews in geophysical imaging (Meju and Gallardo 2016), reservoir seismology (Bosch et al. 2010), hydrogeophysics (Linde and Doetsch 2016), mineral exploration (Lelièvre and Farquharson 2016), petroleum exploration (Moorkamp et al. 2016). Two main ideas underlie these approaches. First, some local structural orientations are inferred from borehole data or other geophysical data to constrain the covariance function used during inversion. Second, a petrophysical model is used to exploit the existing correlation between the physical parameters. As these correlations generally depend on the rock type, the model often includes discrete variables that estimate or sample the rock type at a given location. This notion of rock type is close to the notion of lithofacies, so it is a way to integrate geological reasoning into inverse methods.

In the field of reservoir engineering and hydrogeology, methods incorporating prior geological knowledge in flow and transport models have also been developed very early on, as discussed in several review papers (Farmer 2005; Linde et al. 2015; de Marsily et al. 2005; Oliver and Chen 2011; Zhou et al. 2014a). One fundamental reason is that flow and transport processes can be highly non-linear while pressure and concentration measurements are generally quite sparse as compared to the number of potential factors influencing fluid transfers in porous and fractured media. The same observation holds in potential field inversion, where geological prior information can significantly help addressing the ill-posedness of the inverse problem (Lelièvre and Farquharson 2016). But what does “geological prior” exactly mean?

As noted in particular by Frodeman (1995), geology is an interpretive science which includes a significant component of historical thinking. One aim of geology is to describe the earth in historical terms by identifying the main geological processes and their impact. In terms of scientific philosophy, it is interesting to highlight that geology generally produces refutable scenarios, whereas mathematics are concerned with formal and irrefutable proofs (given some hypotheses). The encounter of these two scientific methods is deeply written in the DNA of Mathematical Geosciences. Advanced methods in physically-based modeling have been developed to quantitatively model geological processes. Some very interesting inverse methods that use such models have been developed recently to quantitatively integrate spatial observations (Charvin et al. 2009; Cross and Lessenger 1999; Gallagher et al. 2009). These methods are ideal in the sense that they could in principle unify geology and geophysics rigorously. However, the interplay of multiple coupled physical and chemical processes at geological time scales remains extremely challenging to model on a computer. The use of such models in an inverse framework is also very challenging, as the number of unknown or poorly known parameters makes the inverse problem highly ill-posed and computationally intractable. This empty space problem is very general and applies to most inverse problems in geosciences, but it is critical when an explicit time dimension is considered because the density of information in time-space is very small (e.g., only a few points typically constrain pressure and temperature in basin studies). This explains why most of the methods in Fig. 28.1e–h do not explicitly consider geological time and instead use an object-based approach, a statistics-based approach or a combination of both to represent the geological prior information and make forecasts in the 3D physical space.

Classically, the object-based strategy is essential to the geological approach. For example, geological mapping typically decomposes a complex reality into discrete and interconnected tectonic, igneous, metamorphic, diagenetic, stratigraphic and sedimentological objects. These object definitions do integrate historical and process-based considerations. For instance, time is explicitly considered in the definition of the remarkable surfaces that sequence stratigraphers use to interpret geoscience data. The characterization of these objects in mathematical and computational terms has been a significant focus of the IAMG for that last 50 years. The statistics-based approach, another clear focus of the IAMG, is clearly complementary to the object-based approach. Indeed, objects are heterogeneous, boundaries between objects may be difficult to define and objects can be difficult to map from available observations. Statistical reasoning is key to address these problems. In this chapter, we will try to explain a few manners by which the object-based and statistics-based methods interact in the frame of geo-data and physical modeling integration. For this, we will start from the perspective of what physical modeling needs.

28.3 Parameterizations for Physical Models

Sambridge et al. (2012), among others, give a very crisp and generic summary of the parameterizations used in most numerical physical modelling methods. In this view, a model \( m\left( {\mathbf{x}} \right) \) is defined at any point \( {\mathbf{x}} \) of the physical space by a set of basis functions:
$$ m\left( {\mathbf{x}} \right) = \sum\limits_{k = 1}^{K} {m_{k} \varphi_{k} \left( {\mathbf{x}} \right)} . $$

For example, in the finite element method with linear triangular elements, a basis function \( \varphi_{k} \) is defined for each mesh vertex \( {\mathbf{x}}_{k} \): \( \varphi_{k} \left( {{\mathbf{x}}_{k} } \right) \) is equal to 1, \( \varphi_{k} \left( {{\mathbf{x}}_{j \ne k} } \right) \) is equal to 0 and \( \varphi_{k} \) linearly decreases in the mesh elements adjacent to \( {\mathbf{x}}_{k} \). The values \( m_{k} \) are the parameter values (e.g., thermal conductivity) associated to the mesh vertices.

The general formulation (28.1) allow to compute or approximate differential operators to solve partial differential equations describing physical processes. Many recent advances in computational physics consist of particular choices of basis functions. For instance, in the extended finite element method, the use of Heaviside basis functions to represent internal discontinuities in a mesh was a step change in the computation of fracture growth (Moës et al. 2002). Another very active research field concerns the combination of basis functions at several scales (e.g., Efendiev et al. 2013). These methods have been applied for instance in finite volume modeling of flow in porous media to solve the flow and transport equations at two distinct and interacting scales (Jenny et al. 2003; Møyner and Lie 2014).

Equation (28.1) is also compatible with the theory of spatial random fields. At point scale, the values \( m_{k} \) are seldom known below the Earth surface. Geostatistics offers many ways to estimate or simulate such values (Chiles and Delfiner 2012; Goovaerts 1997) using statistical parameters inferred from subsurface data. One of these parameters is the variogram, which models the statistical correlation between two variables as a function of the distance. In dual kriging, Eq. (28.1) is also used, as the unknown value is estimated as a linear combination of covariance functions centered on the data points. The use of point-based parameterizations is also much studied in computational physics under the term “meshless methods”, see for instance Liu and Gu (2005). In the practice of geostatistical methods, the values \( m_{k} \) are generally modeled on a Cartesian grid, but recent papers also discuss about the application of geostatistics on unstructured grids (Gross and Boucher 2015; Manchuk et al. 2005; Zaytsev et al. 2016), or directly on points (Zagayevskiy and Deutsch 2016). A major interest of these methods is to estimate or simulate values directly on the physical modeling support, and also to use adaptive resolution depending on the local information density and on the sensitivity between the model parameters and the physical process.

Last, but not least, Eq. (28.1) is compatible with a new breed of inverse methods in which the number of parameters \( K \) is variable, see Sambridge et al. (2012) and references therein. These transdimensional inverse methods show much promise to address some of the challenges highlighted in this chapter.

The beauty of Eq. (28.1) lies in its potential to unify object-based geological descriptions and mathematical descriptions. In a sense, the goal of the various workflows described in Fig. 28.1 and in the associated references can be seen as a quest to find “geological basis functions” to model the earth. The purpose of Sect. 28.4 is to try to establish a more explicit correspondence between geological concepts and existing mathematical and computational models for representing geological domains in three-dimensional space. In doing so, we keep in mind that these 3D models will eventually need to be expressed by Eq. (28.1) in physical models.

28.4 Geological Parameterizations

As discussed in Sect. 28.2, geologists apply the divide and conquer principle to analyze the earth. Hundreds of years of geological reasoning have essentially led to identify multiple geological features at various scales, depending on their origin:
  • Tectonic objects: Faults, joints, folds, cleavages.

  • Sedimentary objects: stratigraphic units, horizons and unconformities, sedimentary bodies, facies, bedding structures.

  • Intrusive and effusive objects: salt diapirs, salt sheets, shale diapirs, shale mounds, sills or dykes, lava flows, etc.

  • Epigenetic objects (originating from chemical and mineralogical processes after rock formation): Metamorphic units, hydrothermalized facies, dissolved rocks (karsts).

These features typically exist at kilometric to micrometric scales (from plates to minerals and fluid inclusions). It is not useful (and not possible) for a model to explicitly represent all objects across these scales. Rather, most modeling approaches hierarchically subdivide the domain to represent a few nested scales (Pyrcz and Deutsch 2014; Ringrose and Bentley 2015).

Two main complementary mathematical and numerical frameworks exist to represent these geological features: spatial random fields and object-based methods. The choice of which framework is most appropriate (or whether and how these frameworks should be combined) depends on the size of the features with regard to the density of observations and on the likely impact of the features for the question at hand. Whereas the object size can be objectively discussed and characterized, the impact of features is often based on rules of thumb derived from experience (Ringrose and Bentley 2015). This may be a source of biases in forecasts. In practical studies, choices may also be constrained by very practical reasons, as some methods are implemented only in commercial software or in distinct software which are not interoperable. These problems and the need for better and abstract knowledge integration are also discussed by Perrin and Rainaud (2013).

28.4.1 Spatial Random Fields

As geological processes are not random and result from many physical processes, the resulting spatial fields are generally correlated in space. The characterization of the correlation structure by statistical inference is an essential aspect of geostatistics (Chiles and Delfiner 2012; Goovaerts 1997). Indeed, trust can be gained when data are numerous enough to provide robust statistics—even though the modeling assumptions themselves may remain questionable (Journel 2005). In inverse modeling of flow and transport in porous media, this has led to many approaches that perturb parameters on a grid while preserving variogram or spatial covariance models (de Marsily et al. 2005; Oliver and Chen 2011; Zhou et al. 2014a).

In geostatistics, a result of the divide-and-conquer strategy used in geology is the definition of many types of discrete categories to describe the physical world. These categories can be localized in space in the form of a geological map (or, in three dimensions, a 3D geological model). From a geostatistical standpoint, categories can be modeled with indicator variables. This has led to significant advances, in particular in the field of multiple-point geostatistics (MPS), to represent discrete facies from sparse data and analog training images. Since the seminal work of Guardiano and Srivastava (1993), a vast community of mathematical geoscientists has embraced this field and made essential advances, see Hu and Chugunova (2008), Mariethoz and Caers (2014). In particular, MPS have opened concrete and effective ways to using complex (and deliberately subjective) geological priors models in inversion (Linde et al. 2015; Melnikova et al. 2015). MPS have shown, in a number of instances, the impact of applying analog reasoning and scenarios to find sensible sets of solutions to inverse problems and to assess uncertainties. They also make up an interesting formalism to analyze complex geological systems (Scheidt et al. 2016).

However, even though progresses can still be made (see for instance Renard et al. 2011), a recurrent challenge with the indicator geostatistical approaches is to ensure that some categories are always connected or adjacent to other categories. This is why, to echo a friendly discussion we had with Andre Journel in 2005, I persist considering that there is more to geological realism than MPS (in its spatial understanding). The Truncated Gaussian method and the Pluri-Gaussian methods (Armstrong et al. 2011), even though they rely on multi-Gaussian assumptions, enforce continuity conditions that approach geological reasoning in a very interesting way. For instance, they can produce consecutive successions of facies from shallow marine to offshore environments. This type of method is appropriate when the discrete geological categories originate from an underlying continuous variable (in the previous example, this variable can be assimilated to bathymetry, all facies being defined between consecutive threshold values). In the Pluri-Gaussian approach, the application of Boolean operations on simulated random fields is also a way to emulate the succession of geological events (e.g. simulation of late diagenetic facies overprinting the depositional facies).

In general, spatial random field methods are implemented on grids of fixed resolution. As a result, the discontinuities that may exist in the medium are sampled at that particular resolution. However, some important features such as fractures or shale lenses may be much smaller than the grid resolution, hence cannot be explicitly represented in the grid. Under some hypotheses, this can be addressed by directly modeling a field of equivalent properties assumed representative of the block scale (e.g., equivalent dual porosity and dual permeability fields in fractured media). However, this can be a source of bias in a number of cases (Jackson et al. 2014). The explicit consideration of these objects generally relies on fewer assumptions and provides a way to deal with more complex geometries and with spatial observations, as will be discussed in Sect. 28.4.2. Note that these two approaches are not mutually exclusive and a combination of both equivalent and explicit approaches are, in general, relevant (Bourbiaux et al. 2002; Maier et al. 2016).

Another important aspect of geological reality is that the orientation and the magnitude of spatial correlation can vary in space. This can be modelled with random fields using locally varying anisotropy (Boisvert et al. 2009; Stroet and Snepvangers 2005; Xu 1996). In geophysics, the use of local anisotropy is illustrated for instance by Clapp et al. (2004) and by the image-guided inversion methods mentioned in Sect. 28.2 and Fig. 28.1d. In the absence of exhaustive data to constrain these orientations, one should estimate or simulate the orientations away from local observations (Gumiaux et al. 2003; Stroet and Snepvangers 2005; Xu 1996). A practical challenge in the presence of locally varying anisotropy is the inference of geostatistical parameters, as the domain is non-stationary. Object approaches offer another way of dealing with locally varying anisotropy, as will be discussed in the next section.

28.4.2 Object Models

In a general sense, object models directly represent the tectonic, sedimentological, intrusive and epigenetic features listed at the beginning of Sect. 28.4. As geological objects originate from distinct geological processes at different periods of time, they often correspond to contrasts or discontinuities of the physical parameters of interest. This explains why, beyond pure cartographic goals, so much effort is dedicated to object modeling in geosciences.

Geometry and Topology

As discussed by Mallet (2002) and Perrin and Rainaud (2013), geological objects can be represented in geometrical and topological terms. Topology refers to essential characteristics: the dimension of objects (line, surface or volume), whether objects have inclusions or holes, and if they are connected to other objects. Depending on the type of geological objects, some topological configurations are impossible (Caumon et al. 2004). For instance, a chronostratigraphic horizon must be an open surface and may include internal holes due to faults or intrusions. More generally, the continuity of objects can have a relation to the genesis of the object, hence is a way to constrain geological models. Knowing what is topologically possible and what is not gives precious insights to design modeling methods and to test the validity of geological models (Pellerin et al. 2017; Wellmann et al. 2014). Topological analysis also provides interesting metrics to characterize and understand geological objects such as karsts (Collon et al. 2017), fracture networks (Sanderson and Nixon 2015) and structural models (Lindsay et al. 2013; Pellerin et al. 2015; Thiele et al. 2016a, b). Last, but not least, topology is very important for flow modeling, as it directly relates to the connectivity of permeability conduits and barriers. The links between connectivity and effective flow properties has been much studied at multiple scales in the frame of percolation theory (Berkowitz and Balberg 1993; King et al. 2001). In the cases where geological considerations are not sufficient to fully characterize the topology of the medium, specific methods have been proposed to find possible object geometry honoring some prescribed connectivity (Borghi et al. 2012; Collon-Drouaillet et al. 2012; Henrion et al. 2010).

Geometry concerns the embedding of the topological objects in 3D space, and is typically described either analytically (e.g., ellipses for fractures) or numerically (using a mesh). Meshes provide much flexibility to discretize the geometry of rock volumes (geological bodies), surfaces (geological boundaries) and lines (contacts between boundaries). All these geometric components are linked by topological relationships (Pellerin et al. 2017). More fundamentally, meshes are a way to define basis functions approximating the geometry of the true object. For example, one can define mathematically a triangulated surface as a set of a “hat” basis functions centered on each surface node (taking the value 1 at each node and linearly decreasing it to zero at the node’s neighbors), as in Eq. (28.1). This description is very powerful to devise advanced geometry processing algorithms and reduce the dimensionality of complex geometrical shapes (Vallet and Lévy 2008). In the frame of inverse modeling, several inverse methods use the meshed model geometry as an unknown parameter (Fullagar et al. 2000; Gjøystdal et al. 1985; Mondal et al. 2010).

Over the past decade, computational advances have also made it possible to consider implicit surfaces to represent geological boundaries. In these approaches, the surfaces are considered as level sets of some three-dimensional scalar field (Calcagno et al. 2008; Cowan et al. 2003; Frank et al. 2007; Henrion et al. 2010). These methods share the same principles as the Truncated Gaussian and Pluri-Gaussian methods (Mannseth 2014), but the underlying random function model is not necessarily Gaussian, and their focus is set on the geometry of object boundaries. These level set methods are very powerful to automate geometric modeling tasks such as interpolation and extrapolation. In particular, they have shown much interest in stratigraphic modeling as one single scalar field can represent a conformable stratigraphic series at once, which opens new possibilities in structural data interpolation (Calcagno et al. 2008; Caumon et al. 2013; Hillier et al. 2014; Laurent et al. 2016). Implicit surfaces also offer very nice ways to consider geometric model perturbations needed to address inverse problems in geosciences (Cardiff and Kitanidis 2009; Caumon et al. 2007; Noetinger 2013; Zheglova et al. 2013). A major distinction between explicit and implicit surface models is about topological control: the surface topology has to be chosen before interpolation in explicit methods, whereas it emerges from the interpolation in implicit models, see also Collon et al. (2016) for more discussions.

As in Pluri-Gaussian simulation, it is possible to indirectly account for geological time in object models using the truncation between implicit or explicit objects (Calcagno et al. 2008; Caumon et al. 2009; Gjøystdal et al. 1985). Boolean operations also provide ways to obtain sharp features in object geometry using constructive solid geometry principles (Rongier et al. 2014; Ruiu et al. 2016). In terms of Eq. (28.1), Boolean operations between implicit objects can be described as indicator (or Heaviside) basis functions (Mannseth 2014; Moës et al. 2002): these functions are equal to zero on one side of the interface and equal to 1 on the other side. The representation of faults is a major challenge which is specific to geosciences. Indeed faults are not just discontinuities or sharp geometric features: they result from sliding of rocks that were previously connected. Several authors have proposed mathematical or numerical solutions to address this problem by considering directly or indirectly the displacement between either sides of a fault (Calcagno et al. 2008; Georgsen et al. 2012; Hale 2013; Holden et al. 2003; Jessell and Valenta 1996; Laurent et al. 2013; Mallet 2002, 2014).

From Objects to Physical Parameters

Generally, geological object geometry cannot be described analytically and determining the associated physical parameter fields is not straightforward. In most cases, objects are first discretized in space with a mesh that will support the numerical resolution of the physical equations (Kolditz et al. 2012; Pellerin et al. 2017). This mesh is a numerical translation of Eq. (28.1) discretizing the space in elementary volumes deemed representative of some effective physical properties (the values \( m_{k} \) in Eq. (28.1)).

A possible working assumption is to consider a constant (or analytically defined) parameter value associated to each type of geological object. This principle is used for simplicity in a number of numerical models (Gjøystdal et al. 1985; Jackson et al. 2015). However, as discussed above, heterogeneity exists at many different scales and can have an impact on the physical process below the scale of the objects that are explicitly represented in a numerical model. For example, it is well known in stochastic hydrogeology and reservoir engineering that petrophysical heterogeneity exists within layers or sedimentary facies and impacts flow and transport (see for instance de Marsily et al. 2005 for a review). In many cases, the orientation of heterogeneities within a geological object depends on the object geometry (e.g., crystal orientations in a dyke may be preferentially aligned along the dyke boundaries; sedimentary heterogeneities tend to be more continuous along layers than orthogonally to layers). This can be addressed in modeling by explicitly using locally variable directions of anisotropy (Boisvert et al. 2009) or by considering a geometric transform between two spaces (Mallet 2014; Shtuka et al. 1996). This last option is very promising as it provides a way to simplify geostatistical modeling, and as it allows to define some useful geological variables such as the apparent sedimentation rate (Kedzierski et al. 2007; Mallet 2014; Massonnat 1999). Such use of indirect geological parameters is an essential and powerful way to introduce geological principles in earth models.

Nonetheless, one should not neglect that object geometry affects model predictions at the two main stages of geostatistical models: (1) geostatistical inference (distributions of continuous variables within each subdomain, multivariate relationships between different variables, trends, spatial variability) and (2) geostatistical modeling (interpolation or simulation). The separation of integrated modeling into an object-modeling phase and a petrophysical modeling phase are, therefore, relatively easy in the classical case where objects are known, when a clear separation of scales exist between representative elementary volume (REV) properties and object geometry, and when objects do not affect geostatistical parameters. However, uncertainty about object geometry and topology can have a significant impact on statistical parameters (Lallier et al. 2016), which can be a significant source of complexity in practical studies. More generally, finding at what scale explicit objects properties and REV effective properties can be separated is a fundamental problem in modeling. Therefore, more research is clearly needed to capture the interactions between object geometric (and topological) parameters and random field parameters.

Object Uncertainty

Geometric uncertainty can be sampled by adding geometric perturbations to an existing reference model (Caumon et al. 2007; Corre et al. 2000; Lecour et al. 2001) or creating several models after perturbing data (Lindsay et al. 2013; Wellmann et al. 2010). As the very existence of some objects is also uncertain in many cases, it is also useful to consider object-based stochastic simulation. In random set theory, geometric objects are placed randomly and independently in the domain by combining the simulation of points (Poisson Point Process) and the simulation of objects shapes around these points (see Chiles and Delfiner 2012 and references therein; Lantuéjoul 2002). Classically, objects are geometric primitives defined analytically, whose shape, orientation and size parameters are simulated from some input distribution. Random set theory places a lot of emphasis on the statistical aspects of this process and on conditioning to spatial data, see in particular Lantuéjoul (2002) and Allard et al. (2006). These models, in particular the Boolean Model, have been used to simulate many types of geological objects such as fractures (Chiles 1988), shale lenses (Haldorsen and Lake 1984) or sedimentary channels (Deutsch and Wang 1996; Holden et al. 1998). Extensions of the Boolean Model have also been proposed to introduce interactions between objects such as attraction or repulsion between fractures to reproduce their mechanical interactions (Aydin and Caers 2017; Bonneau et al. 2016; Chiles 1988; Hollund et al. 2002).

From a random set perspective, a deterministic object model is a particular realization of some underlying random set process. In this case, the relatively large data density allows one to consider mainly the data conditioning problem rather than focusing on the number of objects and on their spatial density. Another focus of deterministic object modeling approaches relates to the expert-guided definition of interactions between objects using interactive editing tools to ensure that the connectivity between objects is compatible with the geological history of the domain (e.g., how faults branch one onto another and how faults displace horizons).

Yet, more and more complex geometric object parameterizations have recently been introduced in object-based simulation methods. For instance, several authors propose to anchor sedimentary channels on discrete polygonal curves (Mariethoz et al. 2014; Pyrcz et al. 2009; Rongier et al. 2017; Ruiu et al. 2016; Viseur 2004). Other variants consider the bounding surfaces of stratigraphic deposits together with some rules to mimic depositional processes (Graham et al. 2015; Labourdette 2008; Michael et al. 2010; Pyrcz et al. 2005, 2015; Rongier et al. 2017; Ruiu et al. 2016; Sech et al. 2009). As argued in the review of Pyrcz et al. (2015), these models make it possible to consider genetic principles such as erosion, progradation and aggradation of sedimentary deposits in an automatic way. Similarly, pseudo-process-based models have also been proposed in the area of fracture modeling to approximate mechanical interactions and truncations that occur during fracture growth (Bonneau et al. 2013; Davy et al. 2013; Srivastava et al. 2005). At a larger scale, a recent trend has been to simulate possible stochastic geometries where the number and the connectivity of faults is variable (Aydin and Caers 2017; Cherpeau et al. 2010, 2012; Cherpeau and Caumon 2015; Holden et al. 2003; Julio et al. 2015a). In all these approaches, the use of rules is often a means to generate realistic objects and to produce likely connectivities and spatial features without being constrained by some input grid resolution. However, conditioning to dense spatial data sets remains challenging with these approaches. A possible way forward is to consider parameter-rich object-models and to consider process-based rules backward in time (Parquer et al. 2016; Ruiu et al. 2015). In all cases, expert control of model realism is also difficult and may call for additional “geological likelihood” functions to scrutinize the realizations (Jessell et al. 2010).

Interestingly, the use of continuous functions around the Poisson points used in object-based simulation (Random Function Model (Jeulin 2002)), is a possible way to relate random sets to Eq. (28.1). However, formalizing the link between object models and basis functions used in physical models is not easy and relies on the assumption that values are analytically defined on each object, and that objects have stationary statistics (Jeulin 2012; Oda 1986). Dealing with more realistic geometries and sequential Boolean operations to reproduce the succession of geological events calls for further numerical and mathematical developments. Meanwhile, as statistical properties of random sets are not easily checked in practical cases, the numerical approach to relate objects to physics clearly remains an area of much interest (Botella et al. 2016; Cacace and Blöcher 2015; Karimi-Fard and Durlofsky 2016; Merland et al. 2014; Mustapha 2011; Pellerin et al. 2014; Zehner et al. 2015).

28.5 Conclusions and Challenges

Several complementary ways exist to incorporate geological information in earth models (Fig. 28.2): spatial statistics, geological variables, geometry and topology of geological objects and explicit geological process modeling. Links exist between the random field and object-based frameworks in cases where the canonical random field theory is applicable (e.g., homogeneous and stationary object densities). This forms the rationale for most modeling methods where “small” objects are treated though their (spatially correlated) equivalent properties at the representative elementary volume scale. “Large” objects are modeled explicitly using rules and parameters that incorporate geological principles and may be calibrated from data and analogs.
Fig. 28.2

Summary of the various complementary ways to incorporate geological knowledge in earth models

Although geostatistics has proven an invaluable theoretical framework to rigorously describe geological domains, it needs to be complemented by geological reasoning (sensu Frodeman 1995). Namely, considering discrete time steps approximating geological history and geological variables which cannot be directly measured can significantly help generating more predictive geological models, which may not always have stationary statistical properties. Geometric and topological interactions between objects have a direct connection to geological history and prove a powerful tool to characterize geological domains.

From a physical modeling perspective, geometric object models allow to represent small spatial features which can have a large impact on physical processes (Jackson et al. 2015; Julio et al. 2015b; Matthäi et al. 2007). This calls for specific developments in meshing and physical simulation, for example to better account for object features directly in the numerical code (Pichot et al. 2012). In the frame of inverse problems, sensitivity analysis is essential in practical studies. Theoretically, specific methods integrating the probability of existence of objects also need to be considered more widely, such as random vector parameterization (Cherpeau et al. 2012), reversible jump Monte-Carlo Markov Chain simulation (Green 1995; Sambridge et al. 2012) or ensemble-based methods (Scheidt and Caers 2009). Both in forward and inverse physical models, an additional and significant challenge is to better characterize the multi-sale interactions between geometrical and petrophysical parameterizations (basis functions and associated parameters values).



The ideas expressed in this chapter owe much to Bruno Lévy, Albert Tarantola, Andre Journel and Jean-Laurent Mallet. Their encouragements, trust and critical remarks have been essential influences. I am also grateful to the graduate students and colleagues of the Research for Integrative Numerical Geology (RING) Team, especially my colleagues Pauline Collon and Paul Cupillard, for their multiple contributions to such a stimulating research environment. Discussions in the frame of the HIWAI ANR project led by Yann Capdeville also fed some of the ideas about scale expressed in this chapter. Last, but not least, at a time where research funding is getting more and more complex, I express my great appreciation to the academic and industrial sponsors of RING-Gocad Consortium for their continued support and to ASGA for its effective Consortium management.


  1. Agterberg F (2014) Geomathematics: theoretical foundations, applications and future developments [Internet]. Springer International Publishing, Cham. Accessed 17 Aug 2015Google Scholar
  2. Allard D, Froidevaux R, Biver P (2006) Conditional simulation of multi-type non stationary Markov object models respecting specified proportions. Math Geol 38(8):959–986CrossRefGoogle Scholar
  3. Armstrong M, Galli A, Beucher H, Loc’h G, Renard D, Doligez B et al (2011) Plurigaussian simulations in geosciences. Springer Science & Business MediaCrossRefGoogle Scholar
  4. Aydin O, Caers JK (2017) Quantifying structural uncertainty on fault networks using a marked point process within a Bayesian framework. tectonophysics [Internet], 2017 May. Accessed 9 May 2017
  5. Berkowitz B, Balberg I (1993) Percolation theory and its application to groundwater hydrology. Water Resour Res 29(4):775–794CrossRefGoogle Scholar
  6. Boisvert JB, Manchuk JG, Deutsch CV (2009) Kriging in the presence of locally varying anisotropy using non-Euclidean distances. Math Geosci 41(5):585–601CrossRefGoogle Scholar
  7. Bonneau F, Caumon G, Renard P (2016) Impact of a stochastic sequential initiation of fractures on the spatial correlations and connectivity of discrete fracture networks. J Geophys Res Solid Earth 121(8):5641–5658CrossRefGoogle Scholar
  8. Bonneau F, Henrion V, Caumon G, Renard P, Sausse J (2013) A methodology for pseudo-genetic stochastic modeling of discrete fracture networks. Comput Geosci 56:12–22CrossRefGoogle Scholar
  9. Borghi A, Renard P, Jenni S (2012) A pseudo-genetic stochastic model to generate karstic networks. J Hydrol 414–415:516–529CrossRefGoogle Scholar
  10. Bosch M, Mukerji T, Gonzalez EF (2010) Seismic inversion for reservoir properties combining statistical rock physics and geostatistics: a review. Geophysics 75(5):75A165–75A176CrossRefGoogle Scholar
  11. Botella A, Lévy B, Caumon G (2016) Indirect unstructured hex-dominant mesh generation using tetrahedra recombination. Comput Geosci 20(3):437–451CrossRefGoogle Scholar
  12. Bourbiaux B, Basquet R, Cacas MC, Daniel JM, Sarda S (2002) An integrated workflow to account for multi-scale fractures in reservoir simulation models: implementation and benefits. In: Abu Dhabi international petroleum exhibition and conference 2002Google Scholar
  13. Cacace M, Blöcher G (2015) MeshIt—a software for three dimensional volumetric meshing of complex faulted reservoirs. Environ Earth Sci 74(6):5191–5209CrossRefGoogle Scholar
  14. Caers J (2011) Modeling uncertainty in the earth sciences. WileyCrossRefGoogle Scholar
  15. Calcagno P, Chilès J-P, Courrioux G, Guillen A (2008) Geological modelling from field data and geological knowledge: Part I. Modelling method coupling 3D potential-field interpolation and geological rules. Phys Earth Planet Inter 171(1):147–157CrossRefGoogle Scholar
  16. Cardiff M, Kitanidis PK (2009) Bayesian inversion for facies detection: an extensible level set framework: level sets for facies detection. Water Resour Res 2009 Oct; 45(10):n/a–n/aGoogle Scholar
  17. Caumon G (2010) Towards stochastic time-varying geological modeling. Math Geosci 42(5):555–569CrossRefGoogle Scholar
  18. Caumon G, Collon-Drouaillet P, Le Carlier De Veslud C, Viseur S, Sausse J (2009) Surface-based 3D modeling of geological structures. Math Geosci 41(8):927–45CrossRefGoogle Scholar
  19. Caumon G, Gray G, Antoine C, Titeux M-O (2013) Three-dimensional implicit stratigraphic model building from remote sensing data on tetrahedral meshes: theory and application to a regional model of La Popa basin, NE Mexico. IEEE Trans Geosci Remote Sens 51(3):1613–1621CrossRefGoogle Scholar
  20. Caumon G, Lepage F, Sword CH, Mallet J-L (2004) Building and editing a sealed geological model. Math Geol 36(4):405–424CrossRefGoogle Scholar
  21. Caumon G, Tertois A-L, Zhang L (2007) Elements for stochastic structural perturbation of stratigraphic models. EAGE Pet, GeostatCrossRefGoogle Scholar
  22. Charvin K, Gallagher K, Hampson GL, Labourdette R (2009) A Bayesian approach to inverse modelling of stratigraphy, Part 1: method. Basin Res 21(1):5–25CrossRefGoogle Scholar
  23. Cherpeau N, Caumon G (2015) Stochastic structural modelling in sparse data situations. Pet Geosci 21(4):233–247CrossRefGoogle Scholar
  24. Cherpeau N, Caumon G, Caers J, Lévy B (2012) Method for stochastic inverse modeling of fault geometry and connectivity using flow data. Math Geosci 44(2):147–168CrossRefGoogle Scholar
  25. Cherpeau N, Caumon G, Lévy B (2010) Stochastic simulations of fault networks in 3D structural modeling. Comptes Rendus Geosci 342(9):687–694CrossRefGoogle Scholar
  26. Chiles JP (1988) Fractal and geostatistical methods for modeling of a fracture network. Math Geol 20(6):631–654CrossRefGoogle Scholar
  27. Chiles J-P, Delfiner P (2012) Geostatistics: modeling spatial uncertainty, 2nd edn. Wiley, Hoboken, N.JCrossRefGoogle Scholar
  28. Clapp RG, Biondi BL, Claerbout JF (2004) Incorporating geologic information into reflection tomography. Geophysics 69(2):533–546CrossRefGoogle Scholar
  29. Collon P, Bernasconi D, Vuilleumier C, Renard P (2017) Statistical metrics for the characterization of karst network geometry and topology. Geomorphology 283:122–142CrossRefGoogle Scholar
  30. Collon P, Pichat A, Kergaravat C, Botella A, Caumon G, Ringenbach J-C et al (2016) 3D modeling from outcrop data in a salt tectonic context: example from the Inceyol minibasin, Sivas Basin, Turkey. Interpretation Aug 4(3):SM17–SM31CrossRefGoogle Scholar
  31. Collon-Drouaillet P, Henrion V, Pellerin J (2012) An algorithm for 3D simulation of branchwork karst networks using Horton parameters and A*: application to a synthetic case. Geol Soc Lond Spec Publ 370(1):295–306CrossRefGoogle Scholar
  32. Corbel S, Wellmann JF (2015) Framework for multiple hypothesis testing improves the use of legacy data in structural geological modeling. GeoResJ 6:202–212CrossRefGoogle Scholar
  33. Corre B, Thore P, de Feraudy V, Vincent G (2000) Integrated uncertainty assessment for project evaluation and risk analysis. In: SPE European petroleum conference. Society of Petroleum Engineers, Paris, FranceGoogle Scholar
  34. Cowan EJ, Beatson RK, Ross HJ, Fright WR, McLennan TJ, Evans TR et al (2003) Practical implicit geological modelling. In: Fifth international mining geology conference, pp 17–19Google Scholar
  35. Cross TA, Lessenger MA (1999) Construction and application of a stratigraphic inverse modelGoogle Scholar
  36. Davis JL, Annan AP (1989) Ground-penetrating radar for high-resolution mapping of soil and rock stratigraphy1. Geophys Prospect 37(5):531–551CrossRefGoogle Scholar
  37. Davy P, Le Goc R, Darcel C (2013) A model of fracture nucleation, growth and arrest, and consequences for fracture density and scaling: a discrete fracture network model. J Geophys Res Solid Earth 118(4):1393–1407CrossRefGoogle Scholar
  38. Deutsch CV, Wang L (1996) Hierarchical object-based stochastic modeling of fluvial reservoirs. Math Geol 28(7):857–880CrossRefGoogle Scholar
  39. Efendiev Y, Galvis J, Hou TY (2013) Generalized multiscale finite element methods (GMsFEM). J Comput Phys 251:116–135CrossRefGoogle Scholar
  40. Elrafie EA, White JP, Awami FH (2008) The event solution–a new approach for fully integrated studies covering uncertainty analysis and risk assessment. SPE-105276-PA. Oct 1 2008Google Scholar
  41. Farmer CL (2005) Geological modelling and reservoir simulation. In: Iske A, Randen T (eds) Mathematical methods and modelling in hydrocarbon exploration and production [Internet]. Springer, Berlin, Heidelberg, pp 119–212. Scholar
  42. Fetkovich MJ (1980) Decline curve analysis using type curves. SPE-4629-PA. June 1, 1980CrossRefGoogle Scholar
  43. Frank T, Tertois A-L, Mallet J-L (2007) 3D-reconstruction of complex geological interfaces from irregularly distributed and noisy point data. Comput Geosci 33(7):932–943CrossRefGoogle Scholar
  44. Frodeman R (1995) Geological reasoning: geology as an interpretive and historical science. Geol Soc Am Bull 107(8):960–968CrossRefGoogle Scholar
  45. Fullagar P, Hughes N, Paine J (2000) Drilling-constrained 3D gravity interpretation. Explor Geophys 31(1/2):17–23CrossRefGoogle Scholar
  46. Gallagher K, Charvin K, Nielsen S, Sambridge M, Stephenson J (2009) Markov chain Monte Carlo (MCMC) sampling methods to determine optimal models, model resolution and model choice for earth science problems. Mar Pet Geol 26(4):525–535CrossRefGoogle Scholar
  47. Georgsen F, Røe P, Syversveen AR, Lia O (2012) Fault displacement modelling using 3D vector fields. Comput Geosci 16(2):247–259CrossRefGoogle Scholar
  48. Gjøystdal H, Reinhardsen JE, Åstebøl K (1985) Computer representation of complex 3-D geological structures using a new “Solid Modeling” technique*. Geophys Prospect 33(8):1195–1211CrossRefGoogle Scholar
  49. Goovaerts P (1997) Geostatistics for natural resources evaluation. Oxford University PressGoogle Scholar
  50. Graham GH, Jackson MD, Hampson GJ (2015) Three-dimensional modeling of clinoforms in shallow-marine reservoirs: Part 1 concepts application. AAPG Bull. 99(06):1013–1047CrossRefGoogle Scholar
  51. Green PJ (1995) Reversible jump Markov chain Monte Carlo computation and Bayesian model determination. Biometrika 82(4):711–732CrossRefGoogle Scholar
  52. Gross H, Boucher AF (2015) Geostatistics on unstructured grid-coordinate systems, connections and volumes, petroleum geostatistics 2015 [Internet]. Accessed 13 Jul 2016
  53. Guardiano FB, Srivastava RM (1993) Multivariate geostatistics: beyond bivariate moments. Geostatistics Troia’92 [Internet]. Springer, pp 133–144. Accessed 30 Apr 2017Google Scholar
  54. Gumiaux C, Gapais D, Brun J (2003) Geostatistics applied to best-fit interpolation of orientation data. Tectonophysics 376(3–4):241–259CrossRefGoogle Scholar
  55. Haldorsen HH, Lake LW (1984) A new approach to shale management in field-scale models. SPE-10976-PA. Aug 1, 1984CrossRefGoogle Scholar
  56. Hale D (2013) Methods to compute fault images, extract fault surfaces, and estimate fault throws from 3D seismic images. Geophysics 78(2):O33–O43CrossRefGoogle Scholar
  57. Henrion V, Caumon G, Cherpeau N (2010) ODSIM: an object-distance simulation method for conditioning complex natural structures. Math Geosci 42(8):911–924CrossRefGoogle Scholar
  58. Hillier MJ, Schetselaar EM, de Kemp EA, Perron G (2014) Three-dimensional modelling of geological surfaces using generalized interpolation with radial basis functions. Math Geosci 46(8):931–953CrossRefGoogle Scholar
  59. Holden L, Hauge R, Skare Ø, Skorstad A (1998) Modeling of fluvial reservoirs with object models. Math Geol 30(5):473–496CrossRefGoogle Scholar
  60. Holden L, Mostad P, Nielsen BF, Gjerde J, Townsend C, Ottesen S (2003) Stochastic structural modeling. Math Geol 35(8):899–914CrossRefGoogle Scholar
  61. Hollund K, Mostad P, Fredrik Nielsen B, Holden L, Gjerde J, Grazia Contursi M et al (2002) Havana—a fault modeling tool. In: Norwegian petroleum society special publications, vol 11, pp 157–71Google Scholar
  62. Hu LY, Chugunova T (2008) Multiple-point geostatistics for modeling subsurface heterogeneity: a comprehensive review: review of multiple POI. Water Resour Res [Internet] 44(11). Accessed 30 Apr 2017
  63. Jackson CA-L, Rotevatn A (2013) 3D seismic analysis of the structure and evolution of a salt-influenced normal fault zone: a test of competing fault growth models. J Struct Geol 2013 Sep 54:215–34Google Scholar
  64. Jackson M, Percival J, Mostaghimi P, Tollit B, Pavlidis D, Pain C et al (2015) Reservoir modeling for flow simulation by use of surfaces, adaptive unstructured meshes, and an overlapping-control-volume finite-element method. SPE-163633-PA. May 1, 2015CrossRefGoogle Scholar
  65. Jackson MD, Hampson GJ, Saunders JH, El-Sheikh A, Graham GH, Massart BYG (2014) Surface-based reservoir modelling for flow simulation. Geol Soc Lond Spec Publ 387(1):271–292CrossRefGoogle Scholar
  66. Jenny P, Lee S, Tchelepi H (2003) Multi-scale finite-volume method for elliptic problems in subsurface flow simulation. J Comput Phys 187(1):47–67CrossRefGoogle Scholar
  67. Jessell M, Ailleres L, De Kemp E, Lindsay M, Wellmann JF, Hillier M et al (2014) Next generation three-dimensional geologic modeling and inversion. Econ Geol 18:261–272Google Scholar
  68. Jessell MW, Ailleres L, de Kemp EA (2010) Towards an integrated inversion of geoscientific data: what price of geology? Tectonophysics 490(3–4):294–306CrossRefGoogle Scholar
  69. Jessell MW, Valenta RK (1996) Structural geophysics: integrated structural and geophysical modelling. Comput Methods Geosci 15:303–324CrossRefGoogle Scholar
  70. Jeulin D (2002) Modelling random media. Image Anal Stereol 2002 21(4):31CrossRefGoogle Scholar
  71. Jeulin D (2012) Morphology and effective properties of multi-scale random sets: a review. Comptes Rendus Mécanique 340(4–5):219–229CrossRefGoogle Scholar
  72. Journel AG (2005) Beyond covariance: the advent of multiple-point geostatistics. Geostat Banff 2004, 225–233Google Scholar
  73. Julio C, Caumon G, Ford M (2015a) Sampling the uncertainty associated with segmented normal fault interpretation using a stochastic downscaling method. Tectonophysics 12(639):56–67CrossRefGoogle Scholar
  74. Julio C, Caumon G, Ford M (2015b) Impact of the en echelon fault connectivity on reservoir flow simulations. Interpretation 3(4):SAC23–SAC34CrossRefGoogle Scholar
  75. Karimi-Fard M, Durlofsky LJ (2016) A general gridding, discretization, and coarsening methodology for modeling flow in porous formations with discrete geological features. Adv Water Resour 96:354–372CrossRefGoogle Scholar
  76. Kedzierski P, Mallet JL, Caumon G (2007) Combining stratigraphic and sedimentological information for realistic facies simulations. EAGE Pet GeostatCrossRefGoogle Scholar
  77. King PR, Buldyrev SV, Dokholyan NV, Havlin S, Lee Y, Paul G et al (2001) Predicting oil recovery using percolation theory. Petroleum Geoscience 7(S):S105–107CrossRefGoogle Scholar
  78. Kolditz O, Bauer S, Bilke L, Böttcher N, Delfs JO, Fischer T et al (2012) OpenGeoSys: an open-source initiative for numerical simulation of thermo-hydro-mechanical/chemical (THM/C) processes in porous media. Environ Earth Sci 67(2):589–599CrossRefGoogle Scholar
  79. Labourdette R (2008) ‘LOSCS’ lateral offset stacked channel simulations: towards geometrical modelling of turbidite elementary channels: lateral offset stacked channels simulations. Basin Res 20(3):431–44Google Scholar
  80. Lallier F, Caumon G, Borgomano J, Viseur S, Royer J-J, Antoine C (2016) Uncertainty assessment in the stratigraphic well correlation of a carbonate ramp: method and application to the Beausset basin, SE France. Comptes Rendus Geosci. 348(7):499–509CrossRefGoogle Scholar
  81. Lantuéjoul C (2002) Boolean model. In: Lantuéjoul C. Geostatistical simulation models and algorithms [Internet]. Springer, Berlin, Heidelberg, pp 153–66. Scholar
  82. Laurent G, Ailleres L, Grose L, Caumon G, Jessell M, Armit R (2016) Implicit modeling of folds and overprinting deformation. Earth Planet Sci Lett 15(456):26–38CrossRefGoogle Scholar
  83. Laurent G, Caumon G, Bouziat A, Jessell M (2013) A parametric method to model 3D displacements around faults with volumetric vector fields. Tectonophysics 1(590):83–93CrossRefGoogle Scholar
  84. Lecour M, Cognot R, Duvinage I, Thore P, Dulac J-C (2001) Modelling of stochastic faults and fault networks in a structural uncertainty study. Pet Geosci 7(S):S31–42CrossRefGoogle Scholar
  85. Lelièvre PG, Farquharson CG (2016) Integrated imaging for mineral exploration. In: Integrated imaging of the earth [Internet]. Wiley Inc, pp 137–66. Scholar
  86. Linde N, Doetsch J (2016) Joint inversion in hydrogeophysics and near-surface geophysics. In: Integrated imaging of the earth [Internet]. Wiley, pp 117–135. Scholar
  87. Linde N, Renard P, Mukerji T, Caers J (2015) Geological realism in hydrogeological and geophysical inverse modeling: a review. Adv Water Resour 86:86–101CrossRefGoogle Scholar
  88. Lindsay MD, Jessell MW, Ailleres L, Perrouty S, de Kemp E, Betts P (2013) Geodiversity: exploration of 3D geological model space. Tectonophysics 594:27–37CrossRefGoogle Scholar
  89. Liu GR, Gu YT (2005) An introduction to meshfree methods and their programming. Springer, Dordrecht; New YorkGoogle Scholar
  90. Ma Y, Hale D, Gong B, Meng Z (Joe) (2012) Image-guided sparse-model full waveform inversion. Geophysics 77(4):R189–198CrossRefGoogle Scholar
  91. Maier C, Karimi-Fard M, Lapene A, Durlofsky LJ (2016) An MPFA-based dual continuum–discrete feature model for simulation of flow in fractured reservoirs. In: ECMOR XV-15th European conference on the mathematics of oil recovery [Internet]. Accessed 14 May 2017
  92. Mallet JL (2002) Geomodeling. Oxford University Press, USAGoogle Scholar
  93. Mallet JL (2014) Elements of mathematical sedimentary geology: the GeoChron model. EAGE publicationsGoogle Scholar
  94. Manchuk J, Leuangthong O, Deutsch CV (2005) Direct geostatistical simulation on unstructured grids. Geostat Banff 2004, 85–94 [Internet]. Springer. Accessed 30 Apr 2017
  95. Mannseth T (2014) Relation between level set and truncated Pluri-Gaussian methodologies for facies representation. Math Geosci 46(6):711–731CrossRefGoogle Scholar
  96. Mariethoz G, Caers J (2014) Multiple-point geostatistics: stochastic modeling with training images. WileyCrossRefGoogle Scholar
  97. Mariethoz G, Comunian A, Irarrazaval I, Renard P (2014) Analog-based meandering channel simulation: Analog-Based Meandering Channel Simulation. Water Resour Res 50(2):836–854CrossRefGoogle Scholar
  98. de Marsily G, Delay F, Gonçalvès J, Renard P, Teles V, Violette S (2005) Dealing with spatial heterogeneity. Hydrogeol J 13(1):161–183CrossRefGoogle Scholar
  99. Massonnat GJ (1999) Breaking of a paradigm: geology can provide 3D complex probability fields for stochastic facies modelling. In: SPE annual technical conference and exhibition. Society of Petroleum EngineersGoogle Scholar
  100. Matthäi SK, Geiger S, Roberts SG, Paluszny A, Belayneh M, Burri A et al (2007) Numerical simulation of multi-phase fluid flow in structurally complex reservoirs. Geol Soc Lond Spec Publ 292(1):405–429CrossRefGoogle Scholar
  101. Meju MA, Gallardo LA (2016) Structural coupling approaches in integrated geophysical imaging. In: Integrated imaging of the earth [Internet]. Wiley Inc, pp 49–67. Scholar
  102. Melnikova Y, Zunino A, Lange K, Cordua KS, Mosegaard K (2015) History matching through a smooth formulation of multiple-point statistics. Math Geosci 47(4):397–416CrossRefGoogle Scholar
  103. Merland R, Caumon G, Lévy B, Collon-Drouaillet P (2014) Voronoi grids conforming to 3D structural features. Comput Geosci 18(3–4):373–383CrossRefGoogle Scholar
  104. Michael HA, Li H, Boucher A, Sun T, Caers J, Gorelick SM (2010) Combining geologic-process models and geostatistics for conditional simulation of 3-D subsurface heterogeneity. Water Resour Res 46(5):W05527CrossRefGoogle Scholar
  105. Moës N, Gravouil A, Belytschko T (2002) Non-planar 3D crack growth by the extended finite element and level sets-Part I: mechanical model: non-planar 3D crack growth-Part I. Int J Num Methods Eng 53(11):2549–2568CrossRefGoogle Scholar
  106. Mondal A, Efendiev Y, Mallick B, Datta-Gupta A (2010) Bayesian uncertainty quantification for flows in heterogeneous porous media using reversible jump Markov chain Monte Carlo methods. Adv Water Resour 33(3):241–256CrossRefGoogle Scholar
  107. Moorkamp M, Heincke B, Jegen M, Hobbs RW, Roberts AW (2016) Joint inversion in hydrocarbon exploration. In: Integrated imaging of the earth [Internet]. Wiley Inc, pp 167–89. Scholar
  108. Mosegaard K (2011) Quest for consistency, symmetry, and simplicity—the legacy of Albert Tarantola. Geophysics 76(5):W51–W61CrossRefGoogle Scholar
  109. Mosegaard K, Hansen TM (2016) Inverse methods. In: Integrated imaging of the earth [Internet]. Wiley Inc, pp 7–27. Scholar
  110. Møyner O, Lie K-A (2014) The multiscale finite-volume method on stratigraphic grids. SPE-163649-PA. Oct 1, 2014CrossRefGoogle Scholar
  111. Mustapha H (2011) G23FM: a tool for meshing complex geological media. Comput Geosci 15(3):385–397CrossRefGoogle Scholar
  112. Nobakht M, Clarkson CR, Kaviani D (2013) New type curves for analyzing horizontal well with multiple fractures in shale gas reservoirs. J Nat Gas Sci Eng 10:99–112CrossRefGoogle Scholar
  113. Noetinger B (2013) An explicit formula for computing the sensitivity of the effective conductivity of heterogeneous composite materials to local inclusion transport properties and geometry. Multiscale Model Simul 11(3):907–924CrossRefGoogle Scholar
  114. Oda M (1986) An equivalent continuum model for coupled stress and fluid flow analysis in jointed rock masses. Water Resour Res 22(13):1845–1856CrossRefGoogle Scholar
  115. Oliver DS, Chen Y (2011) Recent progress on reservoir history matching: a review. Comput Geosci 15(1):185–221CrossRefGoogle Scholar
  116. Paasche H (2016) Post-inversion integration of disparate tomographic models by model structure analyses. In: Integrated imaging of the earth [Internet]. Wiley Inc, pp 69–91. Scholar
  117. Parquer M, Collon P, Caumon G (2016) Conditioning channel backward migration modeling to seismic data. In: 78th EAGE conference and exhibition 2016 proceedings, Vienna, AustriaGoogle Scholar
  118. Pellerin J, Botella A, Bonneau F, Mazuyer A, Chauvin B, Lévy B et al (2017) RINGMesh: a programming library for developing mesh-based geomodeling applications. Comput Geosci [Internet]. Accessed 1 May 2017CrossRefGoogle Scholar
  119. Pellerin J, Caumon G, Julio C, Mejia-Herrera P, Botella A (2015) Elements for measuring the complexity of 3D structural models: connectivity and geometry. Comput Geosci 76:130–140CrossRefGoogle Scholar
  120. Pellerin J, Lévy B, Caumon G (2014) Toward mixed-element meshing based on restricted voronoi diagrams. Procedia Eng 82:279–290CrossRefGoogle Scholar
  121. Perrin M, Rainaud J-F (2013) Shared earth modeling: knowledge driven solutions for building and managing subsurface 3D geological models. Editions TechnipGoogle Scholar
  122. Perrouty S, Lindsay MD, Jessell MW, Aillères L, Martin R, Bourassa Y (2014) 3D modeling of the Ashanti Belt, southwest Ghana: evidence for a litho-stratigraphic control on gold occurrences within the Birimian Sefwi Group. Ore Geol Rev 63:252–264CrossRefGoogle Scholar
  123. Pichot G, Erhel J, de Dreuzy J-R (2012) A generalized mixed hybrid mortar method for solving flow in stochastic discrete fracture networks. SIAM J Sci Comput 34(1):B86–B105CrossRefGoogle Scholar
  124. Pyrcz MJ, Boisvert JB, Deutsch CV (2009) ALLUVSIM: a program for event-based stochastic modeling of fluvial depositional systems. Comput Geosci 35(8):1671–1685CrossRefGoogle Scholar
  125. Pyrcz MJ, Catuneanu O, Deutsch CV (2005) Stochastic surface-based modeling of turbidite lobes. AAPG Bull 89(2):177–191CrossRefGoogle Scholar
  126. Pyrcz MJ, Deutsch CV (2014) Geostatistical reservoir modeling. Oxford university pressGoogle Scholar
  127. Pyrcz MJ, Sech RP, Covault JA, Willis BJ, Sylvester Z, Sun T et al (2015) Stratigraphic rule-based reservoir modeling. Bull Can Pet Geol 63(4):287–303CrossRefGoogle Scholar
  128. Renard P, Straubhaar J, Caers J, Mariethoz G (2011) Conditioning facies simulations with connectivity data. Math Geosci 43(8):879–903CrossRefGoogle Scholar
  129. Ringrose P, Bentley M (2015) Reservoir model design [Internet]. Springer, Dordrecht, Netherlands. Accessed 27 Apr 2017CrossRefGoogle Scholar
  130. Rongier G, Collon P, Renard P (2017) A geostatistical approach to the simulation of stacked channels. Mar Pet Geol [Internet]. Accessed 21 Feb 2017CrossRefGoogle Scholar
  131. Rongier G, Collon-Drouaillet P, Filipponi M (2014) Simulation of 3D karst conduits with an object-distance based method integrating geological knowledge. Geomorphology 217:152–164CrossRefGoogle Scholar
  132. Ruiu J, Caumon G, Viseur S (2015) Semiautomatic interpretation of 3D sedimentological structures on geologic images: an object-based approach. Interpretation 3(3):SX63–SX74CrossRefGoogle Scholar
  133. Ruiu J, Caumon G, Viseur S (2016) Modeling channel forms and related sedimentary objects using a boundary representation based on non-uniform rational B-splines. Math Geosci 48(3):259–284CrossRefGoogle Scholar
  134. Sambridge M, Bodin T, Gallagher K, Tkalcic H (2012) Transdimensional inference in the geosciences. Philos Trans R Soc Math Phys Eng Sci 371(1984):20110547–20110547CrossRefGoogle Scholar
  135. Sanderson DJ, Nixon CW (2015) The use of topology in fracture network characterization. J Struct Geol 72:55–66CrossRefGoogle Scholar
  136. Sava P, Revil A, Karaoulis M (2014) High definition cross-well electrical resistivity imaging using seismoelectric focusing and image-guided inversion. Geophys J Int 198(2):880–894CrossRefGoogle Scholar
  137. Scheidt C, Caers J (2009) Representing spatial uncertainty using distances and kernels. Math Geosci 41(4):397–419CrossRefGoogle Scholar
  138. Scheidt C, Fernandes AM, Paola C, Caers J (2016) Quantifying natural delta variability using a multiple-point geostatistics prior uncertainty model: delta variability and geostatistics. J Geophys Res Earth Surf 121(10):1800–1818CrossRefGoogle Scholar
  139. Sech RP, Jackson MD, Hampson GJ (2009) Three-dimensional modeling of a shoreface-shelf parasequence reservoir analog: Part 1. Surface-based modeling to capture high-resolution facies architecture. AAPG Bull 93(9):1155–1181CrossRefGoogle Scholar
  140. Shtuka A, Samson P, Mallet JL (1996) Petrophysical simulation within an object-based reservoir model. In: SPE-35480-MS. Society of Petroleum Engineers, SPEGoogle Scholar
  141. Srivastava RM, Frykman P, Jensen M (2004) Geostatistical simulation of fracture networks. Geostat Banff 2005:295–304Google Scholar
  142. te Stroet CBM, Snepvangers JJJC (2005) Mapping curvilinear structures with local anisotropy kriging. Math Geol 37(6):635–649CrossRefGoogle Scholar
  143. Thiele ST, Jessell MW, Lindsay M, Ogarko V, Wellmann JF, Pakyuz-Charrier E (2016a) The topology of geology 1: topological analysis. J Struct Geol 91:27–38CrossRefGoogle Scholar
  144. Thiele ST, Jessell MW, Lindsay M, Wellmann JF, Pakyuz-Charrier E (2016b) The topology of geology 2: topological uncertainty. J Struct Geol 91:74–87CrossRefGoogle Scholar
  145. Vallet B, Lévy B (2008) Spectral geometry processing with manifold harmonics. Comput Graph Forum, 251–60. Wiley Online LibraryCrossRefGoogle Scholar
  146. Viseur S (2004) Caracterisation de reservoirs turbiditiques: simulations stochastiques basees-objet de chenaux meandriformes (10 fig.). Bull Soc Geol Fr 175(1):11–20CrossRefGoogle Scholar
  147. Watson TA, Doherty JE, Christensen S (2013) Parameter and predictive outcomes of model simplification: outcomes of model simplification. Water Resour Res 49(7):3952–3977CrossRefGoogle Scholar
  148. Wellmann JF, Horowitz FG, Schill E, Regenauer-Lieb K (2010) Towards incorporating uncertainty of structural data in 3D geological inversion. Tectonophysics 490(3–4):141–151CrossRefGoogle Scholar
  149. Wellmann JF, Lindsay M, Poh J, Jessell M (2014) Validating 3-D Structural models with geological knowledge for improved uncertainty evaluations. European Geosciences Union Assembly 2014 EGU division energy resources and the environment ERE. 59(0):374–381CrossRefGoogle Scholar
  150. Williams GJJ, Mansfield M, MacDonald DG, Bush MD (2004) Top-down reservoir modelling. In: SPE-89974-MS. Society of Petroleum Engineers, SPEGoogle Scholar
  151. Xu W (1996) Conditional curvilinear stochastic simulation using pixel-based algorithms. Math Geol 28(7):937–949CrossRefGoogle Scholar
  152. Zagayevskiy Y, Deutsch CV (2016) Multivariate grid-free geostatistical simulation with point or block scale secondary data. Stoch Environ Res Risk Assess 30(6):1613–1633CrossRefGoogle Scholar
  153. Zaytsev V, Biver P, Wackernagel H, Allard D (2016) Change-of-support models on irregular grids for geostatistical simulation. Math Geosci 48(4):353–369CrossRefGoogle Scholar
  154. Zehner B, Börner JH, Görz I, Spitzer K (2015) Workflows for generating tetrahedral meshes for finite element simulations on complex geological structures. Comput Geosci 79:105–117CrossRefGoogle Scholar
  155. Zheglova P, Farquharson CG, Hurich CA (2013) 2-D reconstruction of boundaries with level set inversion of traveltimes. Geophys J Int 192(2):688–698CrossRefGoogle Scholar
  156. Zhou H, Gómez-Hernández JJ, Li L (2014a) Inverse methods in hydrogeology: evolution and recent trends. Adv Water Resour 63:22–37CrossRefGoogle Scholar
  157. Zhou J, Revil A, Karaoulis M, Hale D, Doetsch J, Cuttler S (2014b) Image-guided inversion of electrical resistivity data. Geophys J Int 197(1):292–309CrossRefGoogle Scholar

Copyright information

© The Author(s) 2018

<SimplePara><Emphasis Type="Bold">Open Access</Emphasis> This chapter is licensed under the terms of the Creative Commons Attribution 4.0 International License (, which permits use, sharing, adaptation, distribution and reproduction in any medium or format, as long as you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license and indicate if changes were made.</SimplePara> <SimplePara>The images or other third party material in this chapter are included in the chapter's Creative Commons license, unless indicated otherwise in a credit line to the material. If material is not included in the chapter's Creative Commons license and your intended use is not permitted by statutory regulation or exceeds the permitted use, you will need to obtain permission directly from the copyright holder.</SimplePara>

Authors and Affiliations

  1. 1.GeoRessources-ENSGUniversité de Lorraine – CNRS–CREGUVandoeuvre-lès-NancyFrance

Personalised recommendations