A laboratory experiment on salt weathering by humidity change: salt damage induced by deliquescence and hydration
Progress in Earth and Planetary Science volume 5, Article number: 84 (2018)
A laboratory experiment on salt weathering was carried out under changing humidity conditions. Three types of rock (tuff and dense and porous sandstone) with sodium chloride, sodium sulfate, or magnesium sulfate were subjected to humidity oscillations from 20%RH to 98%RH during 6 h periods at 20 °C. Prior to the weathering experiment, the rock specimens were oven-dried, and the water supply was restricted to only that from the air during the experiment. Salt on the rock specimens was deliquesced/hydrated at almost 100%RH during the high-humidity period and crystallized/dehydrated during the low-humidity period. Sodium chloride, which has high deliquescence ability, caused the most intensive weathering. Porous sandstone with sodium chloride was completely broken down after 100 cycles of humidity changes. The other two types of rock with sodium chloride showed flaking or swelling on their surfaces. For dense sandstone with sodium chloride, the Equotip rebound value decreased as the humidity cycles increased. Sodium chloride has a high susceptibility of deliquescence at humidities of more than 80%RH. Weathering by sodium chloride would occur extensively on the surfaces of stone heritages and geoheritages in humid coastal spray zones. Magnesium sulfate induced a weight loss in porous sandstone, flaking from the surface of tuff, and cracks on the surface of dense sandstone. Sodium sulfate had almost no effect in the humidity-change experiment, although salt efflorescence was obvious. The results for magnesium sulfate, salt deliquescence, hydration, and crystallization in the humidity-change experiment were easily repeated. Magnesium sulfate might have more influence than sodium sulfate when air humidity fluctuates in a short period.
Salt weathering is one of the major processes of stone decay that causes serious damage to brick walls (Goudie 1977; Kuchitsu et al. 2000), structural foundations (Mottershead 1994; Takahashi et al. 1994), and historical buildings (Gauri 1990; Kamh 2005; Thomachot-Schneider et al. 2011). In natural environments, salt weathering occurs in coastal areas (Matsukura and Matsuoka 1991, 1996; Mottershead 1982), deserts (Cook 1981; Goudie and Cook 1984; Viles and Goudie 2013), and the Antarctic inland (Fahey 1985; Marchant and Head 2007; Miotke 1982; Selby and Wilson 1971). Field observations undertaken globally in a range of environments have suggested the importance of microclimatic conditions in stone decay, including temperature (Hœrlé 2006), insolation (Gunzburger and Merrien-Soukatchoff 2011; McFadden et al. 2005), moisture (Mol 2014), and humidity (Viles 2005).
Many laboratory experiments have simulated salt weathering under the conditions of “cyclic total immersion” or “continuous partial immersion”. In cyclic total immersion experiments, rock specimens are repeatedly subjected to total immersion in a saturated salt solution followed by drying (Goudie et al. 1970; Robinson and Williams 1982; Williams and Robinson 1998). In continuous partial immersion experiments, specimens partly immersed in saturated solutions are subjected to environmental conditions (Goudie 1986; Oguchi and Yuasa 2010; Robinson and Williams 2000). However, these conditions, in which abundant salt water is supplied to the rock specimens, are not likely to occur in the field, with the exception of intertidal zones and places with nearby groundwater. In addition, the drying temperature affects the formation of salt crystals (Aly et al. 2015). The disjuncture between field environments and laboratory experiments has often been pointed out (McGreevy and Smith 1982; Smith et al. 2005).
Air humidity is a water source affecting stone heritages. Arnold and Zehnder (1989) pointed out the importance of monitoring air humidity and temperature for their preservation, as these environmental conditions control salt crystallization and hydration. Goudie and Viles (1997) assumed that air humidity is an important factor in salt crystallization from solution, change of phase (hydration/dehydration), and crystallization pressure. Seasonal salt deliquescence and precipitation have been shown to occur on stone heritages in the presence of air humidity changes (Goudie 1977; Matsukura et al. 2004). In dry areas such as Antarctica and Mars, air humidity is also a major source of water, and salt weathering may be induced by cyclic changes in it (Campbell and Claridge 1987; Gough et al. 2016, 2017; Heinz et al. 2016; Wellman and Wilson 1965). The influence of humidity on hydration/dehydration has been thoroughly examined (Benavente et al. 2004; Rodriguez-Navarro and Doehne 1999; Steiger and Asmussen 2008).
Salt deliquescence occurs when the vapor pressure of a saturated salt solution on salt crystals is less than the vapor pressure of water in the air. Fahey (1985) and Goudie (1993) subjected rock specimens to six different climatic conditions. Both studies suggested that rock breakdown is most intensive under high humidity conditions close to 100%RH. These experimental studies suggested that only salt deliquescence and subsequent salt crystallization could cause the breakdown of rock. However, they partly immersed the rock specimens in water or a salt solution. They also subjected the specimens to humidity changes along with temperature fluctuations.
This study entailed a laboratory experiment on salt damage to rock specimens occurring when humidity fluctuates at a constant temperature. The water source was restricted to only that from air humidity.
Three types of rock (Oya tuff, Aoshima sandstone, and Ubara sandstone) were used. Oya tuff is dacitic or rhyolitic marine pumice tuff of the Miocene age; it was quarried in Utsunomiya, central Japan. In Japan, a variety of buildings and stone statues are made from Oya tuff, which is often damaged by salt weathering (Oguchi and Yuasa 2010). Aoshima sandstone is a very fine-grained, well-cemented sandstone of the Pliocene age; it was collected in the Nichinan Coast, Miyazaki Prefecture, southwest Japan. Ubara sandstone is a fine-grained, weakly cemented, porous sandstone of the Miocene age. The sample was collected on the southeast coast of Chiba Prefecture, central Japan. Tafoni and honeycomb weathering features are well developed on type B shore platforms (Takahashi et al. 1994; Tsujimoto 1987) in these coastal areas and are often associated with salt weathering (Bradley, Hutton, and Twidale 1978; Mustoe 1982; Mottershead 1994; Mottershead and Pye 1994; Strini et al. 2008; Young 1987).
Table 1 shows the physical properties of these rocks. Rock surface hardness was evaluated with the rebound value (L-value) of a type D Equotip hardness tester (Proceq). We used the single impact method, which is one of two methodologies for hardness tests with Equotip (Aoki and Matsukura 2007); this method measures the mean L-values of single impacts at ten different points. The longitudinal wave velocity (P-wave velocity) was measured with an ultrasonic tester (Pundit Plus, CNS Farnell).
Humidity-change weathering experiment
Eight cubic specimens with a side of 5 cm were prepared from the Oya tuff and Aoshima sandstone. Only four cylindrical specimens with a diameter and a height of 3.5 cm were prepared from the Ubara sandstone because of the difficulties in shaping the material into cubes. The initial values of the weight, L-value, and P-wave velocity were measured after oven drying these specimens at 110 °C for 48 h.
Saturated solutions of sodium chloride (NaCl), sodium sulfate (Na2SO4), or magnesium sulfate (MgSO4) were prepared at 20 °C. The rock specimens were immersed with one of the three salt solutions or distilled water for 72 h. After immersion, the specimens were oven dried again at 110 °C for 48 h to provide them with salt prior to the humidity-change experiment.
Each specimen was placed on a sieve with 2 mm openings and was subjected to a total of 200 cycles of humidity changes in an ambient chamber, in which the humidity was oscillated from 20 to 98%RH every 6 h (Figs. 1 and 2). The temperature of the air in the chamber was kept at 20 ± 2 °C during the experiment. Air temperature and relative humidity in the chamber were recorded every 5 min with a data logger (TR-72wf, T&D) with accuracies of ± 5% for RH and ± 0.5% for temperature. The sensor required 7 min to reach a 90% response. Weight, L-value, and P-wave velocity of the specimens were measured every 20 cycles. For Oya tuff and Aoshima sandstone, four specimens were used for measuring the weight; the other four specimens were used for measuring the L-value and P-wave velocity. The L-value and P-wave velocity were not measured in the Ubara sandstone because the specimens were small. All fragments remaining on the sieve were weighed. In addition, the weights of the specimens were measured every hour only for the first humidity-change cycle in order to estimate the amount of water that absorbed from the air on the specimens in the high-humidity period.
Continuous wetting/drying weathering experiment
Another weathering experiment involving repeated wetting/drying with a salt solution was carried out in order to compare its results with those of the humidity-change experiment. Eight cubic specimens each of Oya tuff and Aoshima sandstone were prepared in the same way as in the humidity-change experiment. Four cubes were used for measuring the weight; the other four cubes were used for measuring the L-value and P-wave velocity. After measuring the initial weight or initial L-value and P-wave velocity, the specimens were subjected to a total of 20 cycles of wetting and drying, each of which was composed of the following treatment steps: the specimens were (1) immersed in one of the three salt solutions or distilled water for 24 h at 20 °C, (2) oven dried at 110 °C for 48 h, and (3) immersed in distilled water for 24 h to remove the salt that had crystallized in the specimens. After cooling, they were (4) oven dried again at 110 °C for 48 h and (5) weighed or their L-value and P-wave velocity measured. As in the humidity-change experiment, all fragments remaining on the sieve were weighed.
Results and discussion
Amount of salt in the humidity-change experiment
Table 2 shows the amount of salt contained in the rock specimens for each combination of rock and salt. The porous Oya tuff and Ubara sandstone contained more salt than the Aoshima sandstone did. The amounts of Na2SO4 were smaller than those of the other two salts, which reflected the lower solubility of Na2SO4 (19.0 wt%) than that of NaCl (26.4 wt%) and of MgSO4 (25.2 wt%) at 20 °C.
Salt pathway in the humidity-change cycle
The weights of the rock specimens increased in the high-humidity period and decreased in the low-humidity period. Figure 3 shows that there were significant increases in the weights of the specimens with NaCl during the high-humidity period. The specimens with MgSO4 also showed larger increases than the specimens with Na2SO4 or no salt. The weight increases of the specimens with Na2SO4 were comparable to the values of the specimens with no salt. The weight oscillation means that the rock specimens absorbed water from the air in the high-humidity period, and they dried out in the low-humidity period. At the beginning of the high-humidity period, all three salts appeared to form a solution by dissolving into the water absorbed from the air, indicating that salt deliquescence occurred. The practical deliquescence relative humidity (DRH) at 20 °C is 75.6%RH for NaCl (halite), 83.3–95.1%RH for Na2SO4 (mirabilite), and 92.7%RH for MgSO4 (epsomite) (Apelblat and Korin 1998, 2002; Apelblat and Manzurola 2003). The relative humidity in the ambient chamber rapidly increased and reached almost 100%RH within a few minutes. The high salt content of the rock specimen and low DRH of the NaCl were the causes of the largest weight gain in the high-humidity period.
Hydration also occurred in the high-humidity period. Flatt (2002) and Steiger and Asmussen (2008) described the phase change of Na2SO4. Under the experimental conditions (20 °C), Na2SO4 exists in two stable phases: anhydrate (thenardite) and decahydrate (mirabilite). At the beginning of the experiment, thenardite should crystallize on the rock surface because it directly crystallizes from a saturated solution above 32.4 °C. At the beginning of the high-humidity period, salt deliquescence should cause a saturated solution to form. Because the saturated solution is supersaturated to mirabilite, mirabilite crystallizes from a salt solution (Flatt 2002). In fact, mirabilite crystallized in our experiment 30 min after the first high-humidity period started. In the low-humidity period, mirabilite should crystallize from the solution at 95.6%RH and dehydrate to thenardite below 76.4%RH (Steiger and Asmussen 2008). The crystallization of thenardite is dominant below the equilibrium humidity of 86.6%RH, although both mirabilite and thenardite crystallize directly from solution (Steiger and Asmussen 2008).
The sequence of deliquescence and hydration of thenardite should occur at the beginning of every high-humidity period. However, the deliquescence and phase changes of Na2SO4 were most distinct in the first high-humidity period. These changes became unclear as the number of humidity cycles increased, and the rock surface became covered with the efflorescence of Na2SO4. Kwaad (1970) suggested that the hydration rate of Na2SO4 is much slower than that of MgSO4. Dehydration of mirabilite might hardly have occurred under our experimental conditions, in which the air humidity oscillated over a short interval. Deliquescence of Na2SO4 might have been hindered by the high DRH of mirabilite (95.6% at 20 °C), and efflorescence of Na2SO4 remained on the rock surface.
MgSO4 has three stable hydrated forms: monohydrate (kieserite), hexahydrate, and heptahydrate (epsomite) (Chou and Seal 2003; Vaniman et al. 2004). The hexahydrate is metastable. Though a large number of metastable forms of MgSO4 have been identified besides hexahydrate, the behavior of these metastable forms is still unclear (Chipera and Vaniman 2007). At the beginning of the experiment, kieserite should have crystallized on the rock surface. Steiger et al. (2008) suggested that hydration of kieserite and formation of hexahydrate occur rapidly when the relative humidity exceeds the DRH of kieserite (60%RH at 25 °C), although the reaction proceeds above the equilibrium humidity of kieserite and hexahydrate (42%RH at 25 °C). The rapid reaction occurs as a two-step process of deliquescence and subsequent crystallization. They also reported that epsomite did not form above the equilibrium humidity of hexahydrate and epsomite (51%RH at 25 °C). However, they did not confirm which hydrated crystals form at relative humidities above the DRH of hexahydrate (81%RH at 25 °C). Epsomite would form when the relative humidity exceeds the DRH of hexahydrate. Although we could not distinguish the hydration pathways in our experiment, deliquescence of kieserite and direct crystallization of epsomite would have occurred within a few minutes of exposure to humidity reaching almost 100%RH in the ambient chamber. The epsomite and hexahydrate would have crystallized in the low-humidity period. The kieserite might have occasionally crystallized under the humidity conditions of our experiment (Balboni et al. 2011). Dehydration of epsomite and formation of hexahydrate would also have occurred, whereas the kieserite formation might have been limited by the low equilibrium humidity of hexahydrate and kieserite.
Weight and L-value changes in the humidity-change experiment
Among the three kinds of salt, NaCl caused the most damage to all types of rock in the humidity-change experiment. Ubara sandstone with NaCl was completely broken down after 100 cycles (Figs. 4a and 5a). The cycle 0 data in Fig. 5 refers to the ratio of the weight immediately before the first cycle to the initial salt-free weight; the specimens became heavier from salt precipitation. Oya tuff and Aoshima sandstone did not show any obvious weight losses (Fig. 5a), although a few granular fragments were deposited under the sieve in the cases of the specimens with salt. The samples of Oya tuff with NaCl showed flaking on their surfaces (Figs. 6a), while Aoshima sandstone with NaCl showed swelling on the surface (Fig. 6c). The L-values of the Oya tuff and Aoshima sandstone specimens with NaCl decreased as the number of cycles increased (Fig. 5b). The L-value of these specimens could not be measured after their surfaces became rough. The final L-value was 43.3% of the initial hardness after 120 cycles for Oya tuff and 32.7% after 160 cycles for Aoshima sandstone.
MgSO4 caused the second most amount of damage to the specimens. The weight of Ubara sandstone with MgSO4 decreased to 38.1% of the initial weight after 200 cycles. The samples of Oya tuff with MgSO4 showed flaking on their surfaces (Fig. 6b) and a reduction in their L-value, although the decrease over the first 20 cycles (from 140.3 to 70.9%) was greater than the change in the subsequent 180 cycles (from 70.9% to 45.8%). The decrease in the first 20 cycles was likely induced by salt deliquescence and hydration. The hydration of kieserite and crystallization of the hydrated crystals led to minor rock breakdown and minor changes to the surface micromorphology. These changes caused the L-value to decrease. Aoshima sandstone with MgSO4 had cracks parallel to the rock surface (Fig. 6d). Cracks occurred on the six faces of the cube.
Na2SO4 was relatively inactive as a weathering agent in the humidity-change experiment, with the exception of the weight loss of Ubara sandstone (14.2%) after 200 cycles. The L-value of the Oya tuff with Na2SO4 fluctuated within a range from 84.5 to 101.5%. The L-value of Aoshima sandstone showed indistinct changes, except in the first 20 cycles. The L-value for Aoshima sandstone with Na2SO4 had a similar trend to that with MgSO4. Tabular fragments flaked from the surface of the Oya tuff with Na2SO4 when the specimen was immersed in distilled water after the weathering experiment.
The P-wave velocities of all the specimens were constant or increased slightly during the experiment (Fig. 5c). Only Oya tuff with NaCl recorded a significant decrease from the start to the first 20 cycles.
None of the rock specimens showed any obvious cracks, flaking, or swelling at the beginning of the humidity-change experiment. Therefore, we concluded that the damage caused by the initial immersion in a salt solution and oven drying was relatively weak in comparison with the damage induced by the subsequent humidity changes. The results of the wetting/drying experiment described later supported this conclusion.
The degree of damage induced by each salt was in proportion to the weight gain during the high-humidity period. The lower DRH of NaCl resulted in greater water absorption from the air, and the greater absorption, in turn, induced greater weight losses and L-value reductions. The degree of damage would also have been affected by the fact that NaCl does not hydrate substantially. The hydration of two sulfates involves volume expansion of salt crystals. The hydrated crystals might have filled pores in the rock and hindered infiltration of water (Steiger and Asmussen 2008). The specimens with NaCl could absorb greater amounts of water because NaCl only dissolved and made a solution with deliquescence.
The specimens with Na2SO4 were less damaged than the specimens with MgSO4, despite that the DRH of Na2SO4 was lower than or comparable to the DRH of MgSO4. Ruiz-Agudo et al. (2007) carried out a laboratory experiment on the solutions of Na2SO4 and MgSO4. They reported that Na2SO4 and MgSO4 were both extremely damaging. Balboni et al. (2011) explained that the different behaviors of the two sulfates are due to the different viscosities of their solutions. They assumed that the high viscosity of MgSO4 retards the solution transport and crystal nucleation. High viscosity also causes pores to clog, which retards hydration and deliquescence. In our experiment, as previously mentioned, the slow hydration/dehydration rates of Na2SO4 and the high DRH of mirabilite would have restricted their activity. Na2SO4 is generally regarded as one of the most aggressive salts in both the field and the laboratory (Goudie and Viles 1995, 1997; Smith and McGreevy 1983; Thomachot-Schneider et al. 2011). However, the relative importance of MgSO4 to Na2SO4 might increase in environments in which available water is limited and the humidity is extremely high.
The difference in the water supply method affected how the sulfates induced breakdown of the rocks. Ruiz-Agudo et al. (2007) reported that Na2SO4 caused localized damage and detachment, whereas MgSO4 induced cracks and fractures. Their experiment, in which the lower part of the specimen was immersed in a salt solution, induced salt crystallization inside the rock interior. In contrast, in our experiment, both sulfates concentrated in the surface layer because of the limited water supply from the surface of the rock. Cracking parallel to the rock surface, which occurred in the Aoshima sandstone with MgSO4 and in the Oya tuff with Na2SO4, suggests that salt weathering occurred only within several millimeters of the surface. The interiors were not weathered much because the P-wave velocities of the specimens did not decrease. López-Arce et al. (2011) suggested that porous dolostone is sensitive to diurnal cycles of air humidity at depths up to 3 cm. In our experiment conducted in a short time interval, the depth at which air humidity could have had an effect would have been less than a centimeter from the rock surface.
The specimens with NaCl did not show any cracks. Because NaCl tends to crystallize on the surface, this crystallization pattern is referred to as efflorescence. In contrast, Na2SO4 and MgSO4 tended to crystallize within rock pores, referred to as subflorescence. Salt subflorescence induces greater crystallization pressure than salt efflorescence does (Doehne 2002; Moteershead 2013; Rodriguez-Navarro and Doehne 1999). The difference in the crystallization patterns may be reflected in the absence or presence of cracks on the surface.
Comparison with continuous wetting/drying experiment
The results of the wetting/drying experiment contrasted with those of the humidity-change experiment (Fig. 7). Oya tuff immersed in MgSO4 disintegrated rapidly, and no fragments remained on the sieve after 16 cycles. The L-value of this specimen could not be measured after 2 cycles. Among the Aoshima sandstone specimens, MgSO4 showed the second greatest weight loss and L-value reduction. Although the effect of NaCl was comparable to that of Na2SO4 for Oya tuff, NaCl was obviously inactive for Aoshima sandstone. Na2SO4 substantially damaged the Oya tuff and caused the most damage to the Aoshima sandstone.
The weights of some of the specimens could not be measured after the sieve openings became clogged with rock fragments. In addition, the L-values could not be measured after the surfaces of the specimens became rough.
For Aoshima sandstone specimens with Na2SO4, the final weight was 15.4% of the initial weight after 13 cycles, and the final L-value was 24.1% of the initial hardness after 9 cycles. Oya tuff specimen with Na2SO4 disintegrated rapidly; the final weight was 43.8% of the initial weight after 13 cycles. The L-value of another Oya tuff specimen rapidly decreased; the final value was 44.8% of the initial hardness after 9 cycles. Aoshima sandstone immersed in NaCl did not show any distinct changes in either weight or L-value.
The less hydrated forms of each salt, i.e., halite, thenardite, and kieserite, would crystallize by oven drying at 110 °C. Breakdown and disintegration mainly occurred when the specimens were immersed in distilled water. Hydration of thenardite and kieserite would have occurred during the immersion. We used distilled water in the wetting sequence, whereas the previous experiments often used salt solutions in various concentrations. Thenardite and kieserite in rock specimens dissolve in distilled water, and their solution would have reached saturation as the water penetrated the rock. There was no sign of rock breakdown during the subsequent oven drying and immersion in salt solution, although crystallization and hydration would have been possible if salt remained in the specimens.
As we described above, the dominant weathering processes in the wetting/drying experiment would be salt crystallization of halite and hydration of thenardite or kieserite. These processes are almost the same as those expected in the humidity-change experiment, i.e., deliquescence/recrystallization of halite and hydration of thenardite and hexahydrate of MgSO4. The difference in damage between the two experiments thus did not result from the salt pathways, despite that the crystallization/hydration pressures vary with temperature and humidity (Flatt 2002). The difference between these two experiments was mainly due to the difference in the water supply methods.
Comparison of rock properties
Pore size distribution, micropore volume, and specific surface area generally affect susceptibility to physical weathering (Benavente et al. 2004; Matsukura and Matsuoka 1996; Matsuoka 1990; Ordóñez et al. 1997; Yu and Oguchi 2010; Arnold and Zehnder 1989). The specific surface area probably affects the salt weathering susceptibility by humidity changes because a larger specific surface area causes greater absorption.
Ubara sandstone with higher porosity and lower tensile strength (Table 1) showed the greatest weight losses (Fig. 4). Although Oya tuff has comparable properties to Ubara sandstone, Oya tuff has large pores resulting from the alternation of pumice, while Ubara sandstone is composed of uniform fine sand. These facts imply that the micropore volume and the specific surface area of Ubara sandstone are greater than those of Oya tuff. The differences in micropore volume might have affected the weathering rates in the humidity-change experiment.
This study highlights that salt weathering obviously occurs under conditions in which the water supply is limited to air humidity. The humidity oscillation induced a cycle of repeated salt deliquescence, hydration, and crystallization. The degrees of damage were strongly correlated with the volume of water absorbed in the rock specimens.
NaCl caused the most damage to the specimens. Porous and weak sandstones with NaCl were completely broken down after 100 cycles of humidity change. The other two types of rock also showed concentrated damage on their surfaces. The lower DRH of NaCl resulted in more water being absorbed from the air, which in turn induced greater weight losses and L-value reductions. The absence of hydrated forms would also have facilitated water absorption from the air.
The salt pathways of Na2SO4 would be deliquescence of thenardite and subsequent recrystallization of mirabilite. For MgSO4, deliquescence of hexahydrate and recrystallization of epsomite would also occur. MgSO4 induced damage in all of the rock specimens, whereas Na2SO4 had almost no effect in our experiment. Na2SO4 may be ineffective as an agent of salt weathering in high-humidity conditions. The volume expansion with hydration of Na2SO4 might hinder infiltration of water into the rock. The high DRH of mirabilite would also prevent salt deliquescence.
Aoshima sandstone with MgSO4 developed cracks parallel to its surface that reflected the different crystallization patterns (efflorescence or subflorescence). MgSO4 tends to form subflorescence, unlike NaCl and Na2SO4. The tendency was observed under the condition in which a limited volume of water from air humidity was supplied to the rock surface.
Tafoni, which is often associated with salt weathering, occasionally appears hundreds of meters away from coastlines. In supratidal zones, salts are provided by sea spray on their surface. In such conditions, NaCl is supplied to and precipitates on the rock surface in stormy weather; subsequent humidity fluctuations would induce salt weathering.
Sulfates are often found on building materials, and sodium sulfate is thought to be one of the most aggressive salts. However, the restricted activity of Na2SO4 in our experiment suggests that deliquesce and hydration of Na2SO4 are hindered by the clogging of rock pores with the hydrated salts. MgSO4 did not show such behavior, although deliquesce and hydration of MgSO4 would have occurred. MgSO4 would be more effective than Na2SO4 under conditions in which the water supply is limited to air humidity.
Deliquescence relative humidity
Equotip rebound value
- MgSO4 :
- Na2SO4 :
- P-wave velocity:
Longitudinal wave velocity
Aly N, Gomez-Heras M, Hamed A, Álvarez De Buergo M, Soliman F (2015) The influence of temperature in a capillary imbibition salt weathering simulation test on Mokattam limestone. Mater Constr 65:e044
Aoki H, Matsukura Y (2007) A new technique for non-destructive field measurement of rock-surface strength: an application of an Equotip hardness tester to weathering studies. Earth Surf Proc Land 32:1759–1769
Apelblat A, Korin E (1998) The vapour pressures of saturated aqueous solutions of sodium chloride, sodium bromide, sodium nitrate, sodium nitrite, potassium iodate, and rubidium chloride at temperatures from 227 K to 323 K. J Chem Thermodyn 30:59–71
Apelblat A, Korin E (2002) The vapour pressure of water over saturated solutions of sodium sulfate, calcium bromide, ferric chloride, zinc nitrate, calcium nitrate, and lithium nitrate at temperatures from 278.15 K to 323.15 K. J Chem Thermodyn 34:1621–1637
Apelblat A, Manzurola E (2003) Solubilities and vapour pressures of saturated aqueous solutions of sodium tetraborate, sodium carbonate, and magnesium sulfate and freezing-temperature lowerings of sodium tetraborate and sodium carbonate solutions. J Chem Thermodyn 35:221–238
Arnold A, Zehnder K (1989) Salt weathering on monuments. In: 1st International Symposium on the Conservation of Monuments in the Mediterranean Basin, Bari, 7–10 June 1989
Balboni E, Espinosa-Marzal RM, Doehne E, Scherer GW (2011) Can drying and re-wetting of magnesium sulfate salts lead to damage of stone? Environ Earth Sci 63:1463–1473
Benavente D, Garcı́a del Cura MA, Garcı́a-Guinea J, Sánchez-Moral S, Ordóñez S (2004) Role of pore structure in salt crystallisation in unsaturated porous stone. J Cryst Growth 260:532–544
Bradley WC, Hutton JT, Twidale CR (1978) Role of salts in development of granitic tafoni, South Australia. J Geol 86:647–656
Campbell IB, Claridge GGC (1987) Antarctica: soils, weathering processes and environment. Elsevier, Amsterdam
Chipera SJ, Vaniman DT (2007) Experimental stability of magnesium sulfate hydrates that may be present on Mars. Geochim Cosmochim Ac 71:241–250
Chou I-M, Seal RR (2003) Determination of epsomite–hexahydrite equilibria by the humidity–buffer technique at 0.1 MPa with implications for phase equilibria in the system MgSO4–H2O. Astrobiology 3:619–630
Cooke RU (1981) Salt weathering in deserts. P Geologist Assoc 92:1–16
Doehne E (2002) Salt weathering: a selective review. In: Siegfried S, Thomas W, Axel V (eds) Natural stone, weathering phenomena, conservation strategies and case studies: introduction, Geological Society of London special publication vol 205. Geological Society of London, London, pp 51–64
Fahey BD (1985) Salt weathering as a mechanism of rock breakup in cold climates: an experimental approach. Z Geomorphol 29:99–111
Flatt RJ (2002) Salt damage in porous materials: how high supersaturations are generated. J Cryst Growth 242:435–454
Gauri KL (1990) Decay and preservation of stone in modern environments. Environ Geol Water S 15:45–54
Goudie AS (1977) Sodium sulphate weathering and the disintegration of Mohenjo-Daro, Pakistan. Earth Surf Proc Land 2:75–86
Goudie AS (1986) Laboratory simulation of “the wick effect” in salt weathering of rock. Earth Surf Proc Land 11:275–285
Goudie AS (1993) Salt weathering simulation using a single-immersion technique. Earth Surf Proc Land 18:369–376
Goudie AS, Cooke R, Evans I (1970) Experimental investigation of rock weathering by salts. Area 2:42–47
Goudie AS, Cooke RU (1984) Salt efflorescences and saline lakes; a distributional analysis. Geoforum 15:563–582
Goudie AS, Viles HA (1995) The nature and pattern of debris liberation by salt weathering: a laboratory study. Earth Surf Proc Land 20:437–449
Goudie AS, Viles HA (1997) Salt weathering hazard. John Wiley & Sons, Chichester
Gough RV, Chevrier VF, Tolbert MA (2016) Formation of liquid water at low temperatures via the deliquescence of calcium chloride: implications for Antarctica and Mars. Planet Space Sci 131:79–87
Gough RV, Wong J, Dickson JL, Levy JS, Head JW, Marchant DR, Tolbert MA (2017) Brine formation via deliquescence by salts found near Don Juan Pond, Antarctica: laboratory experiments and field observational results. Earth Planet Sc Lett 476:189–198
Gunzburger Y, Merrien-Soukatchoff V (2011) Near-surface temperatures and heat balance of bare outcrops exposed to solar radiation. Earth Surf Proc Land 36:1577–1589
Heinz J, Schulze-Makuch D, Kounaves SP (2016) Deliquescence-induced wetting and RSL-like darkening of a Mars analogue soil containing various perchlorate and chloride salts. Geophys Res Lett 43:4880–4884
Hœrlé S (2006) Rock temperatures as an indicator of weathering processes affecting rock art. Earth Surf Proc Land 31:383–389
Kamh GME (2005) The impact of landslides and salt weathering on Roman structures at high latitudes—Conway Castle, Great Britain: a case study. Environ Geol 48:238–254
Kushitsu N, Ishizaki T, Nishiura T (2000) Salt weathering of the brick monuments in Ayutthaya, Thailand. Dev Geotech Eng 84:319–327
Kwaad FJPM (1970) Experiments on the granular disintegration of granite by salt action. University Amsterdam Fysisch Geografi sch en Bodemkundig Laboratorium Publicatie 16:67–80
López-Arce P, Fort R, Gómez-Heras M, Pérez-Monserrat E, Varas-Muriel MJ (2011) Preservation strategies for avoidance of salt crystallisation in El Paular Monastery cloister, Madrid, Spain. Environ Earth Sci 63:1487–1509
Marchant DR, Head JW (2007) Antarctic dry valleys: microclimate zonation, variable geomorphic processes, and implications for assessing climate change on Mars. Icarus 192:187–222
Matsukura Y, Matsuoka N (1991) Rates of tafoni weathering on uplifted shore platforms in Nojima-Zaki, Boso Peninsula, Japan. Earth Surf Proc Land 16:51–56
Matsukura Y, Matsuoka N (1996) The effect of rock properties on rates of tafoni growth in coastal environments. Z Geomorphol Supp 106:57–72
Matsukura Y, Oguchi CT, Kuchitsu N (2004) Salt damage to brick kiln walls in Japan: spatial and seasonal distribution of efflorescence and moisture content. B Eng Geol Environ 63:167–176
Matsuoka N (1990) Mechanisms of rock breakdown by frost action: an experimental approach. Cold Reg Sci Technol 17:253–270
McFadden LD, Eppes MC, Gillespie AR, Hallet B (2005) Physical weathering in arid landscapes due to diurnal variation in the direction of solar heating. Geol Soc Am Bull 117:161–173
McGreevy JP, Smith BJ (1982) Salt weathering in hot desert: observation on the design of simulation experiments. Geogr Ann 64A:161–170
Miotke F (1982) Physical weathering in Taylor Valley, Victoria Land, Antartica. Polar Geogr Geol 6:71–98
Mol L (2014) Investigations into the relationship between changes in internal moisture regimes and rock surface deterioration in cavernous sandstone features. Earth Surf Proc Land 39:914–927
Mottershead DN (1982) Coastal spray weathering of bedrock in the supratidal zone at East Prawle. South Devon Field Studies 5:663–684
Mottershead DN (1994) Spatial variations in intensity of alveolar weathering of a dated sandstone structure in a coastal environment, Weston-super-Mare, UK. In: Robinson DA, Williams RBG (eds) Rock weathering and landform evolution. Wiley, New York, pp 151–174
Mottershead DN (2013) Coastal weathering. Treatise on Geomorphology 4:228–244
Mottershead DN, Pye K (1994) Tafoni on coastal slopes, South Devon, U.K. Earth Surf Proc Land 19:543–563
Mustoe G (1982) The origin of honeycomb weathering. Geol Soc Am Bull 93:108–115
Oguchi CT, Yuasa H (2010) Simultaneous wetting/drying, freeze/thaw and salt crystallization experiments of three types of Oya tuff. In: Přikryl R, Török Á (eds) Natural stone resources for historical monuments, Geological Society of London special publication vol 333. Geological Society of London, London, pp 59–62
Ordóñez S, Fort R, García del Cura MA (1997) Pore size distribution and the durability of a porous limestone. Q J Eng Geol 30:221–230
Robinson DA, Williams RBG (1982) Salt weathering of rock specimens of varying shape. Area 14:293–299
Robinson DA, Williams RBG (2000) Experimental weathering of sandstone by combinations of salts. Earth Surf Proc Land 25:1309–1315
Rodriguez-Navarro C, Doehne E (1999) Salt weathering: influence of evaporation rate, supersaturation and crystallization pattern. Earth Surf Proc Land 24:191–209
Ruiz-Agudo E, Mees F, Jacobs P, Rodriguez-Navarro C (2007) The role of saline solution properties on porous limestone salt weathering by magnesium and sodium sulfates. Environ Geol 52:269–281
Selby M, Wilson A (1971) The origin of the labyrinth, Wright Valley, Antarctica. Geol Soc Am Bull 82:471–476
Smith BJ, McGreevy JP (1983) A simulation study of salt weathering in hot deserts. Geogr Ann 65A:127–133
Smith BJ, Warke PA, McGreevy JP, Kane HL (2005) Salt-weathering simulations under hot desert conditions: agents of enlightenment or perpetuators of preconceptions? Geomorphology 67:211–227
Steiger M, Asmussen S (2008) Crystallization of sodium sulfate phases in porous materials: the phase diagram Na2SO4–H2O and the generation of stress. Geochim Cosmochim Ac 72:4291–4306
Steiger M, Linnow K, Juling H, Gülker G, AEl J, Brüggerhoff S, Kirchner D (2008) Hydration of MgSO4•H2O and generation of stress in porous materials. Cryst Growth Des 8:336–343
Strini A, Guglielmin M, Hall K (2008) Tafoni development in a cryotic environment: an example from Northern Victoria Land, Antarctica. Earth Surf Proc Land 33:1502–1519
Takahashi K, Suzuki T, Matsukura Y (1994) Erosion rates of sandstone used for a masonry bridge pier in the coastal spray zone. In: Robinson DA, Williams RBG (eds) Rock weathering and landform evolution. John Wiley & Sons, Chichester, pp 175–192
Thomachot-Schneider C, Gommeaux M, Fronteau G, Oguchi CT, Eyssautier S, Kartheuser B (2011) A comparison of the properties and salt weathering susceptibility of natural and reconstituted stones of the Orval Abbey (Belgium). Environ Earth Sci 63:1447–1461
Tsujimoto H (1987) Dynamic conditions for shore platform initiation. Science Report of the Institute of Geoscience, University of Tsukuba, Sec A 8:45–93
Vaniman DT, Bish DL, Chipera SJ, Fialips CI, Carey JW, Feldman WG (2004) Magnesium sulphate salts and the history of water on Mars. Nature 431:663–665
Viles HA (2005) Microclimate and weathering in the central Namib Desert, Namibia. Geomorphology 67:189–209
Viles HA, Goudie AS (2013) Weathering in the central Namib Desert, Namibia: controls, processes and implications. J Arid Environ 93:20–29
Wellman HW, Wilson AT (1965) Salt weathering, a neglected geological erosive agent in coastal and arid environments. Nature 205:1097–1098
Williams RBG, Robinson DA (1998) Weathering of sandstone by alunogen and alum salts. Q J Eng Geol Hydroge 31:369–373
Yamada T, Aoki H, Takahashi M, Matsukura Y (2005) Effect of rock properties on rates of salts weathering: a laboratory experiment. J Japan Soc Eng Geol 46:72–78 (in Japanese with English abstract)
Young ARM (1987) Salt as an agent in the development of cavernous weathering. Geology 15:962–966
Yu S, Oguchi CT (2010) Role of pore size distribution in salt uptake, damage, and predicting salt susceptibility of eight types of Japanese building stones. Eng Geol 115:226–236
We are grateful to the anonymous reviewers for their helpful and constructive comments that contributed to improving the manuscript.
This study was financially supported by a JSPS Grant-in-Aid for Scientific Research (25560143; principal investigator, N. Matsuoka).
Availability of data and materials
Requests for data should be sent to the contact author.
Both authors declare that they have no competing interests.
Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
About this article
Cite this article
Sato, M., Hattanji, T. A laboratory experiment on salt weathering by humidity change: salt damage induced by deliquescence and hydration. Prog Earth Planet Sci 5, 84 (2018). https://doi.org/10.1186/s40645-018-0241-2