Proposal of a New Parameter for the Weathering Characterization of Carbonate Flysch-Like Rock Masses: The Potential Degradation Index (PDI)
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- Cano, M. & Tomás, R. Rock Mech Rock Eng (2016) 49: 2623. doi:10.1007/s00603-016-0915-2
The susceptibility of clay bearing rocks to weathering (erosion and/or differential degradation) is known to influence the stability of heterogeneous slopes. However, not all of these rocks show the same behaviour, as there are considerable differences in the speed and type of weathering observed. As such, it is very important to establish relationships between behaviour quantified in a laboratory environment with that observed in the field. The slake durability test is the laboratory test most commonly used to evaluate the relationship between slaking behaviour and rock durability. However, it has a number of disadvantages; it does not account for changes in shape and size in fragments retained in the 2 mm sieve, nor does its most commonly used index (Id2) accurately reflect weathering behaviour observed in the field. The main aim of this paper is to propose a simple methodology for characterizing the weathering behaviour of carbonate lithologies that outcrop in heterogeneous rock masses (such as Flysch slopes), for use by practitioners. To this end, the Potential Degradation Index (PDI) is proposed. This is calculated using the fragment size distribution curves taken from material retained in the drum after each cycle of the slake durability test. The number of slaking cycles has also been increased to five. Through laboratory testing of 117 samples of carbonate rocks, extracted from strata in selected slopes, 6 different rock types were established based on their slaking behaviour, and corresponding to the different weathering behaviours observed in the field.
KeywordsPotential degradation index Slake durability test Fragment size distribution Carbonate heterogeneous rock masses Weathering behaviour
In heterogeneous slopes, degradation mechanisms (and the choice of subsequent remedial works to be adopted) are closely linked to the weathering behaviour of the different lithologies which make up the slope. In these slopes, instabilities resulting from differential erosion/degradation are common (Cano and Tomás 2013a, b). This is of most importance in areas with an abrupt topography, where any linear works result in numerous cuttings and slopes. Throughout the service life of a transportation corridor, or any other asset whose construction results in the creation of slopes which are permanently exposed to the atmosphere, these instabilities result in significant maintenance and repair costs, and may pose a significant safety hazard. In the most extreme cases, these processes may trigger the failure of the entire slope, either suddenly or gradually. Additionally, these degradation processes may often be considered as failure mechanisms in their own right, rather than just triggering factors. Thus, the problem of slope stability over time should also be considered, where protection against weathering processes cannot be guaranteed (Mišccevic and Vlastelica 2014).
Normal climatic values of Alicante from 1981 to 2010, AEMET (2012)
Resistance to slaking depends on many different parameters, commonly cited in the literature as; permeability, porosity, adsorption, mineralogy, microscopic texture, microfabric, presence of microfractures, etc. (Gamble 1971; Franklin and Chandra 1972; Richardson and Long 1987; Taylor 1988; Dick et al. 1994; Dick and Shakoor 1995; Martínez-Bofill et al. 2004; Erguler and Ulusay 2009; Kaufhold et al. 2013; Gautam and Shakoor 2015; Cano and Tomás 2015). This makes the characterization of slaking behaviour in rocks using a single parameter extremely complex (Erguler and Ulusay 2009; Gautam and Shakoor 2015).
The slaking susceptibility of clay-bearing rocks is known to influence the stability of heterogeneous slopes, as it may result in differential erosion/degradation. However, not all of these rocks show the same behaviour. Considerable differences in the manner of degradation and time taken to degrade may be observed. For this reason, it is extremely important to link behaviour quantified in the laboratory to that observed in the field, for example, using weathering patterns and weathering profiles (Cano and Tomás 2015).
Different rock masses show a specific response to each particular combination of weathering-related parameters present in situ, and the intensity and rate of this response determines its susceptibility to weathering, as described by Hack (1998). Results obtained using indices derived from Slake tests are generally useful for predicting the performance of different types of rocks qualitatively, although their use for the prediction of quantitative behaviour in field conditions is extremely questionable. However, correlations between slake durability and field performance do exist, as observed by Dick and Shakoor (1995) and Shakoor (1995). In addition, Hack (1998), Hack and Huisman (2002) and Nicholson (2001) have demonstrated that laboratory tests have severe limitations in predicting in situ rock mass performance, especially when discontinuities influence the rock mass behaviour. This should be taken into account when using indices obtained in a laboratory environment.
The Slake Durability test (Franklin and Chandra 1972) is the most widely used test worldwide for determining the relationship between slaking and rock durability. This importance is underlined by its endorsement by the International Society for Rock Mechanics (ISRM 1981). Subsequently, the method was standardized by the American Society for Testing and Materials (American Society for testing and Materials (ASTM) 2004), where the second cycle index (Id2) is denominated the Slake Durability Index, and used to quantify a rock’s susceptibility to slaking. However, the test has numerous disadvantages, which will be discussed in subsequent sections of this paper.
The main aim of this paper is to propose a method for characterizing the weathering behaviour of carbonate lithologies that outcrop in heterogeneous Flysch-like slopes. The aim of the authors is that the method should be simple enough to be easily used in practice. This will be achieved by analysing the changes in the fragment size distribution of the material retained in the drum during the Slake Durability Test (ASTM 2004). This is important, as the test occasionally does not differentiate between rocks with different slaking behaviour, as it only measures the mass of particles smaller than 2 mm lost after each test cycle. This means that any particle larger than 2 mm is retained in the drum, and hence used to calculate the Id index. However, in some cases particles smaller than 2 mm make up a very small percentage of the overall sample mass, but the fraction of the initial sample that is retained in the drum disintegrates into numerous smaller particles. The result is that the Id indices do not correlate with the observed in situ durability.
Erguler and Shakoor (2009) proposed a new method to quantify the nature of rocks. This method quantifies the fragment size distribution of the slaked material, using a “disintegration ratio” calculated for each slaking cycle. This is defined as the ratio between the area under the fragment size distribution curve and the total area encompassing the entire range of the fragment size distribution. Erguler and Ulusay (2009) also suggested a disintegration index that can minimize some of the limitations of slake durability test. The comparison between the disintegration index values measured in the laboratory specimens and those in samples from the same outcrops, exposed to atmospheric conditions for 1 year, showed close agreement. Gautam and Shakoor (2013) proposed a method in which a “disintegration ratio” parameter was calculated from the fragment size distribution curves obtained from samples prepared in a similar manner to those used in the slake durability test, but exposed to natural climatic conditions for 1 year. Subsequently, the same authors (Gautam and Shakoor 2015) compared the laboratory slaking behaviour of common clay-bearing rocks to their slaking behaviour under natural climatic conditions observed during the aforementioned 1-year experimental study. In both studies the same “disintegration ratio” was used.
Similar to the aforementioned studies, this paper aims to evaluate the degradation potential of a sample by analysing changes in the fragment size distribution curves obtained from the material retained in the drum after each slake durability test cycle, up to a total of five cycles. This means that changes in the type, morphology and number of fragments are accounted for. As such, a single parameter for characterizing slaking behaviour is proposed, and the behaviour observed in the laboratory is compared with that observed in the field, under natural climatic conditions.
2 Lithological Setting of the Study Area
2.1 General Framework
The Alicante Flysch sequence (Fig. 1) is composed of pelagic sediments, predominated by sequences of grey marls and thin white marly limestones (hemipelagites) that constitute the rythmite predominated by marls. This sequence may overlap calcarenitic turbiditic episodes. However, the sedimentological complexity of the Flysch formation is even greater because some superposed composite gravitational processes such as mélanges and debrites are also present (Cano and Tomás 2013a).
In this study, five slopes were selected and fully characterized (Fig. 1). 117 intact rock samples were extracted from all of the strata present in the selected slopes and were described in detail in the field. They were geologically classified as: (a) thick bedding calcarenites [Grainstone of turbiditic facies of channel (Ta-b)]; (b) thick bedding calcarenites [grainstone of turbiditic facies of channel (Ta-b) or sheet flood facies (Tb, Tb-c)]; (c) Thin bedding calcarenites [turbiditic thin beds of fan fringe facies (Tb-c-d)]; (d) poorly cemented thin bedding calcarenites [turbiditic thin beds of fan fringe facies (Tb-c-d)]; (e) slightly marly limestones; (f) marly limestones; (g) silty calcareous marls; (h) silty marls; (i) calcareous marls–marls; (j) sheet silty marls; (k) soft marls; (l) sheet marls; (m) soft calcareous mélanges; and (n) calcareous debrites.
2.2 Characterization of Rock Mass Jointing
At regional level, the area is fractured into several blocks linked to several main dextran fault systems, such as the Cadiz-Alicante fault (N70E), which generated N20E oriented folding, the Vinalopo fault system (N155E) and the Socovos fault system (N120E) that generated N70E oriented folding (Guerrera et al. 2006).
The two first sets (J1, J2) exhibit a very large persistence (>20 m), and the isolated blocks present a parallelepiped shape. Their average spacings are 28 and 18 cm, respectively. J3 and J4 present a much lower persistence (1.4 and 2.2 m, respectively) and average spacings of 47 and 25 cm, respectively. J5 presents short to very short persistence (1.1 m) and 60 cm of average spacing.
The sixth set of discontinuities corresponds to bedding, which shows a very large persistence. As the studied slopes are heterogeneous, the bedding has been specifically described for each of the lithologies outcropping in the study area. Typically, the thick bedding calcarenites units are 25–120 cm thick and the bedding spacing is 7–30 cm. They are thick bedded blocky, consisting of tabular blocks formed by two to five other intersecting discontinuity sets. The size and shape of these blocks is different to other, less competent lithologies. This is because some discontinuities are well cemented, behaving as if there were no such discontinuity. The slightly marly limestones units are 12–60 cm thick, the bedding spacing is 10–30 cm and they are prismatic blocky. The calcareous mélange units are 50–200 cm thick and exhibit a chaotic structure with a high erratic discontinuity surfaces density that results in heterometric rock blocks (centimetric to decimetric) with different morphologies. The thin bedding calcarenites (C) units are 5–20 cm thick, the bedding spacing is 3–10 cm and they are very blocky with prismatic shape. The thin bedding calcarenites (L) units are 5–30 cm thick and the bedding spacing is 3–10 cm. They are thin bedded blocky consisting of parallelepipedic blocks. The only observed unit of calcareous debrites in the studied slopes is 600 cm thick and exhibits a chaotic structure constituted by blocks and a calcareous matrix with a high erratic discontinuity surfaces density that generates heterometric rock blocks (centimetric to decametric block size) with different morphologies. The only unit of soft calcareous mélange encountered is 20 cm thick and has a chaotic structure. Thin bedding silty calcarenites units are 2–50 cm thick, the bedding spacing is 2–10 cm. They are thin bedded blocky consisting of parallelepipedic blocks. The marly limestones units are 10–80 cm thick and the bedding spacing is 8–30 cm. They are very blocky with prismatic shape, in the same manner as the other lithologies listed below. The silty calcareous marls units are 15–50 cm thick and the bedding spacing is 8–15 cm. The silty marls units are 20–70 cm thick and the bedding spacing is 10–14 cm. The calcareous marls–marls units are 15–160 cm thick and the bedding spacing is 9–30 cm. The sheet silty marls units are 30–160 cm thick and the bedding spacing is 10–23 cm. Soft marls are 25–40 cm thick and the bedding spacing is 10–15 cm.
Regarding openings, it should be noted that in the studied rock masses the presence of infilling in the openings of discontinuities, which are extension joints (not veins), highly depends on the lithology of the unit. As such, only in the following lithologies, which showed high contents of carbonate, are discontinuities filled by free crystals of calcite: thick bedding calcarenites, slightly marly limestones, calcareous mélange, thin bedding calcarenites (C), calcareous debrites, marly limestones, silty calcareous marls and soft calcareous mélange. In these carbonatic lithologies, the opening of joint J1 varies between 0.5 and 10 mm and is completely or partially filled by calcite. The width of J2 ranges from very tight (<0.1 mm) to open (1 mm) and the filling is also made of calcite that can partially fill the discontinuity space or even not be present, leading to a partially open to open discontinuity. Opening ranges are from 0.5 to 5 mm for J3 and from 0.1 to 3 mm for J4. In both cases, the joint is filled or partially filled by calcite. J5 exhibits 1 to 3 mm calcite infilling width (Fig. 2b). Otherwise, in the marly lithologies, the discontinuities also present an aperture varying between <0.1 mm to 10 mm, but without calcite infill. Finally, the joints that correspond to bedding are mainly very tight or they are cemented in the more calcareous lithologies. Additionally, a patina of iron oxide and manganese oxide species in dendritic form has been commonly observed in all sets of discontinuities, including bedding.
Both intact rock and discontinuities exhibited a weathered state, from the face of the slope to certain depth. The degree of alteration changed according to the lithology and the depth, according to Cano and Tomás (2015).
Generally, both, the tectonic discontinuities and the bedding are planar, mainly rough or sometimes slightly rough in the more carbonatic lithologies and smooth or slightly rough in the marly lithologies. Occasionally, the tectonic discontinuities of the units of thick bedding calcarenites, mainly the thickest ones, show evidence of karstification, which generates more undulated or stepped, and very rough joints, and also greater apertures (20 mm). Occasionally, the bedding surface presents load casts at the bottom of calcarenite units of metric thickness at the contact with marly lithologies, generating very rough joints with large undulation. Sometimes, the bedding presents slickensided surfaces.
Water flow was not observed, although after downpours the discontinuities and the intact rock of marly lithologies were wet.
The effect of the excavation method on the disturbance of a rock mass is a well-known phenomenon (Romana 1993; Hoek et al. 2002). However, a large number of factors can influence the degree of disturbance in the rock mass surrounding an excavation, and it may never be possible to quantify these factors precisely (Hoek et al. 2002). Four of the five studied slopes were excavated using mechanical methods and the fifth slope is a natural hill. Due to the heterogeneous nature of these slopes, when the cuts are excavated by means of mechanical methods, the low competence lithologies (e.g., soft marls, silty marls, etc.) are sheared through the rock matrix. However, in the high competence sets (e.g., thick bedding calcarenites) the blocks are broken off through their discontinuities, dislocating them towards the slope face. This is the reason why in the slope face of these sets, the aperture of the discontinuities is higher than that observed in the inner part of the slope, in which the blocks have not been perturbed by the mechanical action of the excavation (Fig. 2c, d). Another cause of the greater discontinuity opening in the more competent blocks from the slope face is the dislocation of rock blocks due to removing underlying unit effects of erosion and/or differential degradation.
3.1 General Overview
3.2 Intact Rock Mineralogy
In this study, the different lithologies were described in the field using a simplified geological classification of rocks based on their genetic classification, structure, composition and grain size (Geological Society of London 1977). Additionally, a mineralogical characterization of the samples by X-ray diffraction was performed. Because some of the samples were of marly composition, they were characterized in two different stages. Firstly, X-ray diffractograms of all the samples were obtained. Secondly, X-ray diffractograms of the oriented aggregate of samples with high phyllosilicate content were obtained, to identify them according to Robert and Tessier’s (1974) methodology. Finally, for some representative samples, the carbonate contents obtained from the interpretation of the X-ray diffractograms were compared with those obtained using the Bernard calcimeter test (ASTM 2007a), to validate these results.
Data were collected and interpreted using the XPowder software package, (Martin 2004) whose qualitative search-matching procedure was based on the ICDD-PDF2 database.
3.3 Assessment of Fragment Size Distributions After the Slake Durability Test
The Slake Durability Test (SDT) is one of the simplest tests in rock mechanics, and is the most widely used test worldwide for characterizing the environmental weathering resistance of rock. Although originally the slake durability test was developed for testing the weathering potential of shales, mudstones, siltstones, and other clay-bearing rocks (Franklin and Chandra 1972), the slake durability index is also typically used for testing weak rocks such as mudstones, marls, ignimbrites, conglomerates, and poorly cemented sandstones (Sabatakakis et al. 1993; Santi 1998; Czerewko and Crips 2001; Erguler and Ulusay 2009; Miščcević and Vlastelica 2011). Consequently, although in the Flysch formation there are some very competent, hard turbiditic rocks that show very high durability indices, to classify the Flysch lithologies using a uniform weathering potential criteria, the slake durability test was used for testing all of the samples.
The durability of weak rocks is usually assessed using the second-cycle slake durability index (Id2). Nevertheless, some authors (Gamble 1971; Taylor 1988; Moon and Beattie 1995; Ulusay et al. 1995; Bell et al. 1997; Gökçeoğlu et al. 2000; Erguler and Shakoor 2009; Miščcević and Vlastelica 2011) have suggested that index values taken after three or more cycles of slaking and drying may be useful when evaluating higher durability rocks, such as those in this study.
As part of a previous study, it was observed that within the study area some intact rock samples showed high Id1 and Id2 indices [after Franklin and Chandra (1972) and Gamble (1971)], in contrast with the weathering behaviour observed in situ. As such, it was concluded that the observed weathering of the rocks was much higher than that predicted by the SDT indices (Cano and Tomás 2015).
The American Society for Testing and Materials requires that as part of the slake durability test, in addition to the Id2 index, the fragments retained in the drum should be qualitatively categorized as type I material (primarily large fragments), type II material (mixture of large and small fragments), or type III material (primarily small fragments) (American Society for testing and Materials (ASTM) 2004). However, Erguler and Shakoor (2009) demonstrated these categories are insufficiently detailed to give a refined classification. As a consequence, it is obvious that the Id2 index does not adequately reproduce the real degradation properties of the Flysch lithologies studied, providing optimistic values.
It should be noted that rock specimens found on superficial parts of slopes usually show signs of weathering or even severe degradation. As a consequence, the Flysch rock samples tested correspond to intact rocks that were obtained from the inner part of the slope. Subsequently, the intact rock samples were transported to the laboratory in plastic bags, and maintained at a constant temperature. The time between storage and testing was always less than 1 week. While the tests were performed, the laboratory temperature was also kept constant (24 ± 2 °C) to conserve humidity and temperature conditions.
The tests were performed according to the ASTM (2004), with five test cycles performed. Five cycles were chosen because of: (a) the need to compare hard and soft lithologies using the same parameter; (b) the existence of some durable rocks which are unaffected by a low number of cycles; (c) the need to study the rocks’ long-term weathering behaviour; and (d) the need to avoid an excessively long test period.
It is unrealistic to classify carbonate Flysch lithologies according to their in situ weathering behaviour after long-term exposure to real conditions based solely on the indices obtained from the slake durability test. As such, many authors have combined (in various different ways) the results of the slake durability test with the analysis of particle size distribution curves (Erguler and Shakoor 2009; Erguler and Ulusay 2009; Gautam and Shakoor 2013, 2015), with the aim of improving the characterization of various lithologies according to their weathering behaviour.
The procedure adopted as part of this study was as follows. Firstly, ten 40–60 g pieces of intact rock were taken from the study area, providing a total sample mass of 450–550 g. The samples were dried for 24 h in an oven at 105 °C, sieved, and immediately placed in the slake durability test apparatus. After the first test cycle, the sample retained in the drum was dried, sieved and weighed. This procedure was repeated for a further four cycles, giving a total number of five test cycles. The sieving procedure adopted for determining fragment size distribution curves was the same as that used for soils (ASTM 2007b), using standard sieves whose aperture sizes were 40, 31.5, 25, 20, 12.5, 10, 6.3, 5 and 2 mm. The results were plotted in semi-logarithmic scale, to show the fragment size distribution of samples before and after each test cycle. The curves were plotted on the same graph, to easily observe changes in the samples after each slaking cycle. The sieve apertures used were shown on the x-axis in semi-logarithmic scale, and the percent passing (by weight) on the y-axis. It is important to note that the samples were sieved with extreme care, to avoid further fragmentation of the particles retained in the drum, which could have been mistakenly attributed to the effects of the previous slaking cycle.
The values calculated for the samples in this study vary from 0.8 to 46, with a value of PDI = 5.7 calculated for the example in Fig. 6.
Standardised qualitative factors used to describe the behaviour of the fragments retained in the drum throughout the five slaking cycles [adapted from ASTM (2004)]
R1 The edges of the fragments appear similar to before the test cycles, or show slightly blunted edges
R2 The edges of the fragments appear completely blunt or lightly rounded. The initial appearance of the fragment may still be noted
R3 The fragments show a rounded shape. The initial shape of the particle is not visible
Variation in number of fragments
Increasing The number of fragments increases significantly from one cycle to the next
Equal The number of fragments is largely constant from one cycle to the next. Small pieces occasionally break off from the corners of the largest fragments and very occasionally a large fragment breaks into two medium sized fragments
Reducing The number of fragments reduces significantly from one cycle to the next
Large fragments (L) The entire sample is composed of large fragments, with occasional smaller fragments
Small fragments (S) The sample is composed primarily of small fragments
Mixture of large and small fragments (M) The sample is composed of a mixture of fragments of different sizes, which may or may not be rounded
Slaking behaviour patterns based on changes observed in the fragments retained in the drum
R3 type roundness of fragments from the first to the last cycle. Initial increase in number of fragments of different sizes (M), maintaining or reducing the number of fragments throughout the test cycles. Fragments of differing size (M) present
Initial R2 type roundness, changing to R3 from the second or occasionally the third cycle. Initial increase in number of fragments of differing size (M), with the number of fragments constant or decreasing throughout subsequent cycles. Fragments of differing size (M) present
Fragments show R2 roundness until the third cycle, occasionally the second. From the fourth or last cycle the roundness type is R3. In the two first cycles the number of fragments of differing size (M) increases, which is maintained or reduces throughout the following cycles. Habitually during the last or fourth cycle, the smallest fragments tend to disappear, leaving a type L sample
R2 type roundness is observed from the first cycle until the fourth, without any increase in the number of fragments, with these being large (L). Occasionally small fragments are generated which tend to disappear in the subsequent cycles. During the fifth cycle the fragments show a more rounded shape (R2 or R3) with very blunt edges
Samples retain their initial number of fragments, which have a similar size (L), throughout the five cycles. Occasionally small fragments break off from the corners, or even larger fragments. The roundness of the fragments is type R1 until the third or fourth cycle, and type R2 in the last or last two cycles
The samples retain the same number of fragments, and of similar size (L) throughout the five cycles of the Slake Durability Test. Occasionally, small fragments break off from the corners. The roundness of the fragments is type R1 in all cycles, although on occasion R2 roundness is observed during the last cycle
These samples show very limited roundness, as they tend to fracture into flat fragments which slide within the drum
Extensive fracturing during the first cycle, into fragments of differing sizes (M), with type R2 roundness observed in the largest fragments and R3 roundness in small- and intermediate-sized fragments. Throughout the following cycles the number of particles of differing sizes (M) is constant or reduces, and the number of fragments with R3 roundness increases
During the first cycle very little fracturing is observed, but during the second cycle a greater degree of fracturing is observed, producing fragments of differing size (M), with an R2 type roundness. During subsequent cycles, the number of fragments of differing size is constant or reduces. From the third or fourth cycle some fragments with type R3 roundness are observed
Fracturing into fragments of differing sizes (M) is observed during the first two cycles, although the initial large fragments predominate, showing R1 roundness. Throughout subsequent cycles the number of particles of differing sizes (M) is constant or reduces, with the smaller fragments tending to disappear, resulting in a type L sample. From the fourth or fifth cycle R2 roundness is observed
Throughout the first two cycles some small fragments are produced, which are maintained or tend to disappear. However, the large initial samples predominate (L–M or L), showing R1 roundness. From the third cycle until the final cycle mixed roundness is observed, with some fragments showing type R1 and others R2
Poorly cemented samples
The poorly cemented calcarenite samples behaved in a distinct manner, as rounding of the original fragments was predominant as opposed to fragmentation
Fragments show type R3 roundness throughout all cycles. The number of large particles (L) is maintained after each cycle, although a reduction in diameter is observed
A qualitative analysis of the changes in morphology in the six fragment size distribution curves obtained for each sample after five slake durability test cycles was performed. The curves showing a similar morphology were grouped.
Using all of the aforementioned parameters (behaviour in terms of changes in the retained fragments, changes in the shape of the fragment size distribution curves, and principally the potential degradation index parameter), all of the samples taken as part of the study were classified, and limits between the different classes were established.
Once all of the samples were classified, the behaviour of the different lithotypes from which the samples were extracted was studied and compared with the weathering patterns and weathering profiles defined by Cano and Tomás (2015).
4 Slake Behaviour Classification: Potential Degradation Index (PDI)
As discussed in the previous section, changes in the DRP parameter throughout the slake durability test cycles were evaluated for 117 samples (Fig. 6). The R2 values and typical error were calculated for the logarithmic curves fitted to each sample. All of the curves showed a good fit, with an average R2 value of R2 = 0.977 ± 0.023, and an error of e = 0.05 %.
Classification of samples based on the Potential Degradation Index (PDI)
Maximum % Passing 12.5 (P12.5)
Patterns (Table 2)
Field weathering profile (Cano and Tomás 2015)
1. Very low
Sheet marls (1), soft marls (3), calcareous marls–marls (1), sheet silty marls (1)
Sheet silty marls (4), calcareous marls–marls (6), poorly cem. thin bedding calc. (1), Thin bedding silty calc. (1), silty calcareous marls (1)
AB (poorly cemented samples
LM (laminated samples)
Thin bedding calcarenites (L) (3), calcareous marls–marls (14), marly limestones (2), soft calcareous mélange (1), silty marls (3), silty calcareous marls (2), thin bedding calcarenites (C) (1), thin bedding silty calc. (1)
LM (laminated samples)
Calcareous marls–marls (5), calcareous debrites (1), Marly limestones (8), thin bedding calc. (L) (2), thin bedding calc. (C) (1), silty marls (2), thick bedding calc. (1)
LM (laminated samples)
Slightly marly limestones (15), marly limestones (2), silty calcareous marls (1), calcareous mélange (3), thin bedding calc. (L) (1), thin bedding calc. (C) (5), Silty marls (1), Thick bedding calc. (1)
LM (laminated samples)
6. Very high
Slightly marly limestones (10), thin bedding calc. (L) (1), thick bedding calc. (9), thin bedding calc. (C) (1), calcareous mélange (1)
5 Field Weathering Characterization
The final part of this study consists of comparing the slaking behaviour of the different samples, based firstly on the analysis of changes in the fragments retained in the drum (see Tables 2, 3; Fig. 7), secondly on the calculation of the potential degradation index, and finally by attending to the weathering patterns and weathering profiles of the different lithologies, as observed in the field by the authors of this study. The field observations of the different lithologies were made for rock that had been exposed to natural climatic conditions over a long period of time. The weathering patterns are defined as follows [based on Cano and Tomás (2015)]:
Not weathered (NW); slight discoloration (A); reduction by arenization (B); flat weathering front peeling off (C); conchoidal peeling off (D); incipient rounding of blocks formed by tectonic joints (E); ellipsoidal morphology blocks formation (F); cubic centimetre fracturing of ellipsoidal block (G); incipient conchoidal fracture of ellipsoidal blocks and formation of ellipsoidal blocks of minor size (H); total conchoidal exfoliation of ellipsoidal blocks (I); massive fracturing in centimetric pseudocubic blocks (J); residual soil (K); centimetric rhomboidal fracturing in centimetric thickness strata (L); and massive fracturing of centimetric thickness strata (M). The field weathering profile is comprised of the sum of different weathering patterns (e.g. FHIJK, EFG, etc.) and in the field it was observed that weathering profiles depended on the lithological nature of the strata, although some lithologies showed similar weathering profiles (Table 4).
6 Results, Analysis and Discussion
The proposed classification is based on the PDI, although to help define the limiting values for each class, the changes in shape of the fragment size distribution curves were also used. Additionally, the P12.5 parameter correlated very well with the PDI, and is less laborious to obtain. As such, this parameter is proposed as an alternative to be used by practitioners.
In addition, the behaviour of the fragments retained in the drum throughout the slaking cycles was studied for each of the 117 samples. As commented previously, this behaviour varied depending on whether the samples showed a compact, laminated or poorly cemented texture. Where the samples were compact, the slake behaviour patterns C1–C5 corresponded directly with the first five proposed classes, giving an FHIJK or EFG weathering profile. The laminated samples behaved differently, as the fragments could not become rounded owing to the fact that they slid around the drum. The slake behaviour patterns of the laminated samples (L1–L4) corresponded to classes 2–5, respectively. The least durable laminar samples (class 1) behaved in a similar manner to the least durable compact samples (i.e. type C1), and in the same way the most durable laminar samples (class 6) behaved similarly to type C6 samples (Table 4).
The samples with an AC weathering profile (the most durable as observed in the field) had a slaking behaviour class equal or greater to “medium” (class 3), and their slake behaviour pattern was always one type greater than that which would be expected for rocks of their class, except for class 6, where they coincided. Where the samples were poorly cemented, the behaviour during the slake cycles was also unusual as the fragments only degraded by rounding, without fracturing and maintaining the same number of fragments (although reduced in size). These samples corresponded to Class 2. Finally, class 6 samples always showed a C6 type slake behaviour pattern, independently of whether they were laminar or compact, and corresponded to the most durable weathering profiles (NW-A, AC, EFG and LM) (Table 4).
Slaking classification of Alicante’s carbonate Flysch lithotypes
Mineralogy and classes of durability →
Very low (PDI ≤ 1.5)
Low (PDI: 1.5–3)
Medium (PDI: 3–5.5)
Medium–high (PDI: 5.5–8)
High (PDI: 8–15)
Very high (PDI > 15)
Thick bedding calcarenites
92.5 ± 4.2
5.4 ± 3.0
2.1 ± 1.6
Slightly marly limestones
82.9 ± 3.2
12.5 ± 2.5
4.6 ± 1.2
87.5 ± 2.4
9.3 ± 1.9
3.2 ± 0.6
Thin bedding calcarenites (C)
78.3 ± 5.4
14.7 ± 3.7
7.0 ± 2.5
Thin bedding calcarenites (L)
72.1 ± 9.8
18.5 ± 7.2
3.3 ± 2.3
84.8 ± 0.0
11.2 ± 0.0
4.0 ± 0.0
79.0 ± 2.6
15.3 ± 2.4
5.7 ± 0.7
Silty calcareous marls
82.4 ± 3.9
12.7 ± 2.1
5.0 ± 1.9
74.7 ± 3.1
17.8 ± 2.6
7.6 ± 0.7
75.0 ± 3.2
17.5 ± 2.6
7.5 ± 1.1
Soft calcareous mélange
84.2 ± 0.0
11.7 ± 0.0
4.2 ± 0.0
Thin bedding silty calc.
70.0 ± 11.7
20.0 ± 9.7
10.1 ± 2.1
Sheet silty marls
68.5 ± 6.8
21.4 ± 6.6
10 ± 1.4
Poorly cem. thin bedding calc.
74.7 ± 0.0
19 ± 0.0
6.4 ± 0.0
75.4 ± 3.8
16.7 ± 3.0
7.7 ± 0.9
75.7 ± 3.7
16.9 ± 2.5
6.5 ± 0.0
If the range of Id2 values is analysed and compared with the proposed new PDI parameter, it may be clearly observed that the use of Id2 overstates the slaking resistance of the carbonate samples in this study by at least one class.
The different samples, classified in six categories based on their PDI, have been also associated with their maximum percent of sample passing through the 12.5 mm sieve (P12.5), the slake behaviour patterns of fragments during five test cycles, the field weathering profile and Id2 index. Additionally, the lithotypes have been associated with their corresponding classes, including the number of samples and allowing the most representative lithologies corresponding to each class to be shown (Table 4).
If the results are analysed according to lithotypes, a clear relationship may be observed between carbonate content and durability—although this is not the determining factor, for reasons discussed previously. However, there is a general trend in the slaking behaviour (classes 1–6) of each lithological group. The thick bedding calcarenites mainly showed a “very high” durability, with a type C6 slake behaviour pattern, corresponding to the NW-A field weathering profile. Slightly marly limestones exhibited a high or very high durability, their slake behaviour pattern was type C5 and C6 and corresponded to the EFG field weathering profile. Calcareous mélange mainly showed a “high” durability, with a type C5 and C6 slake behaviour pattern, corresponding to the AC field weathering profile. Thin bedding calcarenites (compact) mainly exhibited “high” durability, their slake behaviour pattern was type C5, corresponding to the AC field weathering profile.
The behaviour of the thin bedding calcarenites (laminated) was highly variable, oscillating between “medium” and “very high” durability. Their slake behaviour pattern was also variable, although it corresponded exclusively to the LM field weathering profile. When sampling from the slopes in the study area, only one layer of Calcareous debrites was detected, which were classified as “medium–high” durability. No data were available for the slake behaviour pattern, and the field weathering profile was AD.
Marly limestones mainly exhibited “medium–high” durability, their slake behaviour pattern was type C4, corresponding to the EFG field weathering profile. The behaviour of the Silty calcareous marls was very variable, as values indicating both “low” and “high” durability, and intermediate classes, were obtained. Data on the slaking behaviour pattern were not available, and the field weathering profile was exclusively FHIJK. The behaviour of the silty marls also varied greatly, as they were classed as having “medium” to “high” durability. Data on the slaking behaviour pattern were not available, and the field weathering profile was EFG, exclusively. The calcareous marls–marls varied between “low” and “medium–high” durability, with a type C2–C4 slake behaviour pattern. However, the majority of the samples exhibited a “medium” durability with a type C3 slake behaviour pattern, corresponding exclusively to the FHIJK field weathering profile.
The only sample of soft calcareous mélange detected in this study showed a “medium” durability, slake behaviour pattern C3 and corresponded to the LM field weathering profile. The thin bedding silty calcarenites had a “low” to “medium” durability, L1–C3 slake behaviour pattern and LM field weathering profile. Sheet silty marls mainly exhibited a low durability. Their slake behaviour pattern was type C2, which corresponded to the FHIJK field weathering profile. The only sample of poorly cemented thin bedding calcarenites detected in the study area showed a low durability. The slake behaviour pattern was type R, corresponding to the AB field weathering profile. Finally, soft marls and sheet marls were the least durable lithotypes, with a “very low” durability, and a type C1 slake behaviour pattern which corresponded to the FHIJK field weathering profile (Table 5).
The classification of carbonate rocks according to their slaking behaviour using the Idi indices (Franklin and Chandra 1972; Gamble 1971) does not accurately reflect the weathering behaviour observed in situ. The use of only one sieve size (2 mm) in the laboratory does not adequately explain slaking behaviour, since the study of the fragments retained in the drum shows evidence of degradation which is not reflected in the results given by the slake durability test.
A new index based on changes in the disintegration ratio (DRP; Eq. (1), Fig. 5) throughout five slaking cycles—the potential degradation index [PDI; Eq. (3)] has been proposed as an alternative to the Id2 index. This index takes into account the degradation of the sample fragments retained in the 2 mm drum, as well as changes in these fragments throughout the experimental process. This has allowed six durability classes to be established to describe slaking behaviour: very low, low, medium, medium–high, high and very high durability. These classes also agree more closely with weathering behaviour patterns observed in the field.
The results indicate that the Id2 index overstates the slaking resistance of the carbonate rock samples tested by at least one class.
This methodology has also allowed the samples to be grouped according to slake behaviour patterns, which take into account changes in morphology in the fragments retained in the drum after each cycle. Additionally, these parameters have been related to the field weathering profiles defined by Cano and Tomás (2015), which allowed the results of laboratory slake tests to be compared with weathering resulting from long-term exposure to natural climactic conditions observed in the field.
Additionally, a correlation has been proposed between the potential degradation index (PDI) and the maximum percentage of sample passing through the 12.5 mm sieve (P12.5), which is a less laborious parameter to obtain, and hence is considered to be more adequate for practitioners.
This work was funded by the University of Alicante under the project GRE14–04, the Ministerio de Economía y Competitividad del Gobierno de España in the framework of the projects TIN2014-55413-C2-2-P and TEC2011-28201-C02-02. The authors wish to express their sincere thanks to Dr. T. Miranda for comments made during Dr. M. Cano’s stay at the University of Minho (funded by the University of Alicante), which have substantially improved this work.
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