Biocrusts are important functional units in dryland ecosystems. Regarded as ecosystem engineers, cyanobacteria in biocrusts contribute several major physico-chemical and biological processes. However, the role of cyanobacteria in the process of loess formation has been underestimated. Recently, their contribution to sediment development was presented in the BLOCDUST model of loess formation.
This perspective paper features the environmental impact of cyanobacteria and biocrusts with a focus on processes involved in the formation of loess sediments. We propose that the formation of loess can be mediated by cyanobacteria, including initial trapping, and the accumulation and preservation of loess-forming particles. Moreover, the initial structure may be further altered by weak mineral weathering, dissolution and mineral re-precipitation due to cyanobacterial metabolic processes. Possible negative aspects of environmental impact related to the potential toxicity of cyanobacterial biocrusts are also discussed. We highlight specific biotic-abiotic interactions between biocrusts and loess (e.g. exudation of organic polymers, carbonate dissolution and re-precipitation, and dust-dependent metabolic activities of cyanobacteria) which are essential for the formation of stabilized loess and propose the term “synergosis” to comprise these interactions.
The role of cyanobacteria in loess formation has only recently been recognized and the possible biogenic nature of loessification is underestimated as compared to their eolian nature. Mineral weathering and mineral precipitation processes as well as mineral dust flux between litho- and atmosphere mediated by cyanobacteria and biocrusts require more attention due to their significant contribution to ecosystem properties.
Throughout the world, drylands are the most often encountered biotopes of biocrusts (Makhalayane et al. 2015; West 1990), where they can cover up to 70% of the surface (Buis et al. 2009; Karnieli et al. 2002). Biocrusts are present on all seven continents and in all climatic regions (Belnap and Lange 2003). They are particularly significant in the ecology of arid and semi-arid regions (Belnap 2006; Chamizo et al. 2012; Kidron et al. 2010). Biocrusts represent associations of sediment/soil particles with bacteria, cyanobacteria, algae, fungi, lichens and mosses (Belnap and Lange 2003; Chamizo et al. 2012; Evans and Johansen 1999; Hu et al. 2002a) and their secreted metabolites (primarily exopolysaccharides) (Lan et al. 2012), as well as microfauna (Pócs et al. 2006). As a highly productive microenvironment, biocrusts establish and control basic physico-chemical processes of the ground surface, influencing environmental properties at micro and macro scales. Biocrusts also influence soil development, hydrological processes, water and energy balance, nutrient content, soil temperature, movement of gases, eolian particle (dust) uptake and deposition and eventually, plant community development (Weber et al. 2016).
Biocrust diversity is characterized by spatial and temporal variability (Williams et al. 2013), resulting in a succession of autochthonous life forms, with cyanobacteria being common components (Belnap 2001; Lan et al. 2013). The abundance of cyanobacteria in biocrusts of arid and semi-arid regions distributed around the world is significant (Colesie et al. 2016, Fig. 9.4). The cyanobacteria observed in biocrusts belong to at least 48 genera, of which 8 genera are present in all investigated regions (Colorado, Southeastern Utah, Northwestern Ohio, Mexico, India, Southern Africa, Israel, Iran and Spain) (Online Resource 1).
Xerotolerance is one of the major ecophysiological adaptations shaping microbial communities in arid and semi-arid conditions. Cyanobacteria tend to dominate microbial populations in desert biocrusts (Makhalayane et al. 2015; Potts 1994), reflecting their successful survival strategies against desiccation, the ability to cope with transient changes between hot/dry and warm/humid conditions, and versus exposure to high irradiance by visible and UV light (Whitelam and Codd 1986). Cyanobacteria can function as primary colonizers via their ability to grow photoautotrophically and the capacity of some members to fix atmospheric nitrogen. Surface colonization can be further enabled by the production of exopolymeric substances (EPS) leading to biofilm formation or to complex, multilayered microbial mats. Cyanobacterial EPS contains sulphate groups and uronic acids, which give the EPS an anionic and sticky character (Rossi and De Philippis 2015). The EPS layer also minimizes water loss and reduces UV irradiation reaching the cells, thus protecting against abiotic stress factors. Microalgae and mosses are generally unable to function as primary colonizers of constrained environments themselves, and depend on cyanobacteria to provide stable hydrated microenvironments with necessary nutrients (Zhang et al. 2015). In addition, cyanobacteria possess extensive metabolic responses that help them to cope with fluctuations in moisture and irradiance, and to pass through active-dormant-active transitions. Efficient protection of macromolecules constitutes one survival strategy of extremophilic and extremotolerant cyanobacteria. Protein denaturation in water-deficient cells is prevented by the accumulation of osmolytes including, intracellular sucrose and trehalose in drought-resistant cyanobacteria (Hershkovitz et al. 1991). Further defense mechanisms are used against reactive oxygen species (ROS) which cause damage to membranes, nucleic acids and proteins (Whitelem and Codd 1986; Billi and Potts 2002). ROS generation is accelerated under typical dehydrating conditions, i.e. strong sunlight/UV irradiation. Damage by ROS is partly controlled by cyanobacterial Fe-superoxide dismutase that neutralizes formed superoxide radicals (Shirkey et al. 2000). To prevent ROS generation by UV, cyanobacteria synthesize UV-absorbing scytonemin (Garcia-Pichel and Castenholz 1991) and mycosporine-like amino acids (MAAs) (Cockell and Knowland 1999; Garcia-Pichel and Castenholz 1993; Rastogi et al. 2014).
The role of biocrust cyanobacteria in sediment particle accumulation and preservation of land surfaces has long been recognized (Belnap and Gardner 1993). The BLOCDUST hypothesis (Biological LOess Crust – DUSt Trapping) (Svirčev et al. 2013) postulates the role of cyanobacterial biocrusts in the process of loess formation. According to this hypothesis, the accumulation/growth of loess sediment in arid and semi-arid regions is supported via the trapping and accumulation of airborne dust particles during wet events by sticky cyanobacterial EPS. Intervening dry periods provide conditions for the preservation of particles captured and covered by firm biocrusts.
Loess and related deposits are one of the most widespread Quaternary aeolian sedimentary formations, most abundant in semi-arid regions of inner Eurasia (Muhs 2013; Smalley et al. 2011). They present and preserve parent material for the synsedimentary formation of soils, such as fertile chernozem. Moreover, loess has a more applied role and presents a widespread building ground with specific geotechnical properties (Sprafke and Obreht 2016). Despite its importance, the processes required for loess formation are still not fully understood (Sprafke and Obreht 2016). Loess is usually defined as eolian sediments formed by the accumulation of wind-blown dust particles. However, this definition does not cover post-depositional processes related to the formation of loess structure. Typically, loess sediments have homogenous and highly porous structures, with particles loosely cemented by microcrystalline calcium carbonate derived from corrosion and re-precipitation of detrital carbonates (Muhs 2007; Muhs and Bettis 2003; Pésci 1990; Smalley et al. 2006). The formation of a typical loess structure is usually attributed to a process called loessification. Unfortunately, this process is still poorly understood because it is related to processes similar to pedogenesis (neo-formation of clays and Fe-oxides, and carbonate re-precipitation) and diagenesis (cementation of the particles and stabilization of sediment structure), placing loessification in between those processes (Pécsi 1990, 1995; Sprafke and Obreht 2016). In addition, the mechanisms of particle entrapment during dust accumulation are not fully understood. The role of cyanobacteria within biocrusts and processes related to their activity, however, have the potential to explain the processes of particle entrapment, accumulation and preservation. Here, we propose processes facilitated by cyanobacteria and their relation to loess formation. Besides construing the bio-geological importance of cyanobacteria and biocrusts, this article proposes distinct definitions of some ambiguous key terms and introduces a new term: “synergosis”. Further, the possible health significance of dust particle accumulation and of toxins potentially produced by biocrust cyanobacteria is also discussed.
Biological loess crusts and biological loess mats
There is a lack of clear definitions in the terminology of biological crusts. According to some definitions, biocrusts are characterized by periodical or permanent surface features influenced by factors including soil structure and type, irradiance, topographic attributes (Belnap 1995; Hu and Liu 2003; Lange et al. 1997; Zaady et al. 2000), mineral resources and water (Pickett and McDonnell 1989). We refer to a biocrust as a hardened, crisp structure formed by drying, consisting of living but dormant, highly specialized organisms in close association with sediment/soil particles. In describing the changes in biocrust physical properties, some language problems can lead to the use of terms that are redundant (pleonasms) or even contradictory. It can be easily observed that environmental changes between dry and wet events readily lead to a shift between the desiccated and hydrated appearance of biocrusts. In this context “dry biocrust”, the term commonly used in the literature, is pleonastic and “wet biocrust” is contradictory.
When a biocrust becomes hydrated and active due to wetting, it can act as a biological terrestrial mat, a fully functional biological community. The early-developmental stages of hydrated biocrusts (Zhang 2005) improve the surface microenvironment, which in turn provides further aid to colonization and supports the survival of later successional stages (Acea et al. 2003; Hu and Liu 2003; Kurina and Vitousek 1999; Langhans et al. 2010; Lukešová 2001). By synthesizing significant amounts of EPSs, cyanobacteria can promote further growth of the microcommunity and may enable protozoa, small invertebrates and microfungi to become established. Biological terrestrial mat development continues until a climax community is established under given environmental conditions. Further successional steps may lead to the formation of vegetation (if the wet period continues) or the community may reverse to the crust stage (if dry conditions return).
So far, biocrusts have been referred to by multiple names (cryptogamic, microbiotic, cryptobiotic and microphytic crusts) indicating some common features of the constituent organisms, but the most often-used term is “biological soil crust” (BSC) (Belnap et al. 2003a; Langhans et al. 2009). Many factors can be used to classify BSCs (Belnap 2003a; Berkeley et al. 2005; Dougill and Thomas 2004; Langhans et al. 2009; Pócs 2009) but especially important are the physicochemical properties of the growth surface (Chamizo et al. 2012). Regarding this factor, the question arises as to whether the term biological soil crusts can be used for all biocrusts. Declaring all biocrusts as soil crusts can lead to misunderstandings in both a scientific and etiological sense. Crust types differ from physical crusts to biocrusts, where different biological crust types can be described and called by specific names: biocrusts formed on soil, loess, sand, rocks and other substrates, differing in physical and chemical properties.
While substrates, such as unconsolidated sediments (e.g. sand), and sedimentary, metamorphic or magmatic rocks are provided with a clear definition of their structure and genesis, this is not the case with the loess substrate. The specificity of loess lies in its polygenetic nature (Sprafke and Obreht 2016), determined by complex environmental sedimentary and post-depositional processes (Svirčev et al. 2013). While the process of loess formation remains to be fully understood and defined, it is certain that quasi-pedogenic and quasi-diagenetic processes have determined its present structure (Smalley and Marković 2014). Due to its high specificity, loess cannot be regarded either as a weakly consolidated sediment, soil, or rock, but as a distinct entity (Sprafke and Obreht 2016). For example, dust deposited to marine or lacustrine sediments is not loess because of the absence of the loessification process.
In this regard,we propose the terms biological loess crusts (BLC) and biological loess mats (BLM) for consideration (Fig. 1). The length of dry and wet events, and shifting frequencies between BLC and BLM have an effect on initial processes of loessification, as discussed below.
The role of cyanobacterial BLC and BLM in the process of loessification
The BLOCDUST model
By the 1990s, it was concluded that loess is “not just the accumulation of dust” (Pécsi 1990) and a discussion on (abiotic) cementing agents of silt particles emerged (Sprafke and Obreht 2016). However, biocrusts are known to trap airborne dust and consequently cement it, as a part of the life strategy of crust organisms (Danin and Ganor 1991; Pietrasiak et al. 2014; Williams et al. 2012; Zaady and Offer 2010). The accumulated dust particles contribute to the growth- and further strengthen the cohesion of BLC and BLM (Hu et al. 2002a; Felde et al. 2017). In a field study (Zaady and Offer 2010), cyanobacterial crust components were shown to provide a unique contribution to the loess desert ecosystem by significantly enhancing atmospheric particle accumulation. According to the BLOCDUST hypothesis (Svirčev et al. 2013), loess sediment growth in arid and semi-arid regions is facilitated in the same manner, via trapping and accumulation of airborne dust particles by sticky EPS during wet events (Fig. 2). The particles are then processed through a series of weathering reactions, and translocated downward as cyanobacteria move up toward the light source. When biological activity halts during the dry period, the trapped particles remain immobilized and turn into constituents of cohesive BLC that resists wind erosion. The switch between the wet and dry conditions and associated processes represents one cycle of accumulation. The compilation of such cycles results in the initial growth of loess.
The BLOCDUST hypothesis describes and emphasizes the role of BLC and BLM cyanobacteria in the process of initial loess formation and stabilization in arid and semi-arid environments. Stabilization of the soil surface mediated by cyanobacteria within biocrusts has been documented in numerous studies (Table 1). The stabilized soil surface is characterized by an enhanced compressive strength and a higher resistance to accumulated raindrop kinetic energy than that of bare soils. Two main mechanisms of stabilization are distinguished: the immobilization of soil particles through an extensive filamentous network (coarser particles) and the adhering of particles on the EPS surface (finer particles). Through their EPS, cyanobacterial communities enhance cementation between the trapped particles through bioweathering, mineral disaggregation and subsequent mineral precipitation. Current knowledge of these processes within biocrusts is meager and necessitates more studies, both in the field and laboratory. An overview of the weathering processes in lithic environments related to biocrusts is presented in Garcia-Pichel et al. (2016).
The complex structure of cyanobacterial EPS includes extracellular polysaccharides, organic acids (e.g. uronic acids), UV protective pigments, proteins, nucleic acids, lipids, reactive functional groups (e.g. sulphates, phosphates) and peptides. Such composition provides EPS with favorable properties for the bioweathering and mineral disaggregation of trapped particles mainly through the activity of incorporated organic acids (Viles 1995). The chemical composition of EPS is not enough to cause weathering of mineral particles itself: specific micro-environmental conditions are also required. The basic metabolic processes of aerobic respiration and photosynthesis regulate the O2/CO2 ratio and establish oxidizing/reductive, alkaline/acidic microenvironments respectively, which further promote mineral dissolution in the contact zone of the EPS with mineral particles. The required micro-environmental conditions for weathering of minerals depend upon their crystalline structure (Wolff-Boenisch et al. 2006), with carbonates having higher weathering rates than silica minerals. Cyanobacteria-driven dissolution of carbonates is considered to occur during aerobic transpiration, providing increased CO2 concentration and a slightly reductive, acidic environment (Danin 1983; Garcia-Pichel 2006). In some cyanobacteria, dissolution is also supported by a highly specific Ca2+ uptake and transport mechanism driven by P-type Ca2+-ATPases (Garcia-Pichel et al. 2010; Ramírez-Reinat and Garcia-Pichel 2012).
Contrary to carbonates, siliceous substrates are of a much lower weathering rate, primarily due to high Si-O bond abundance, which tends to be the strongest and most resistant to dissolution. However, weathering of silicates in sandstones in arid landscapes mediated by cyanobacteria was observed by Büdel et al. (2004) and a similar scenario of silica weathering was predicted to occur in cyanobacteria-dominated desert biocrusts (Garcia-Pichel and Belnap 1996).
Bioweathering in terrestrial environments mediated by cyanobacteria is recognized as a survival mechanism (Gorbushina 2007). In BLC communities, the airborne particles present the main source of essential mineral nutrients (Svirčev et al. 2013). Through weathering of mineral particles including feldspars, muscovite, amphiboles, pyroxenes, apatite and dolomite, cyanobacteria acquire bio-essential elements (Ca, Na, K, P, Mg, Fe) of which Fe2+ is crucial for photosynthetic activity (Rubin et al. 2011).
The change in redox conditions of the microenvironment from acidic to alkaline caused by cyanobacterial photosynthesis and silicate weathering induces the subsequent precipitation of carbonates from formerly dissolved detrital carbonate and atmospheric CO2 (Goudie and Viles 2012). The alkaline state of EPS induces the deprotonation of functional groups providing binding sites for cations (e.g. Ca2+, Mg2+, Fe2+) (Braissant et al. 2003), while their binding is further supported by the uronic acids present (Braccini et al. 1999). The capacity of EPS to bind cations can be saturated in the case of their constant supply when all of the available functional groups of the polymer are occupied. The remaining available cations combined with alkaline micro-environmental conditions can initialize nucleation of carbonate species on the surface of the EPS in the contact zone with mineral particles (Dupraz et al. 2009), providing a mineral cement between the particles and the EPS (Fig. 3) which is crucial for the permanent immobilization and preservation of the particles.
The EPS-influenced organomineralization presented here occurs as a passive, biologically-influenced process, driven by changes in the physical state of the organic exopolymer (Dupraz et al. 2009; Trichet and Défarge 1995). Microbial organomineralization commonly appears in sedimentary biofilms found in aquatic environments (Gallagher et al. 2010) and was recently recognized in cyanobacteria-dominated BLC (Dulić et al. 2017).
Chemical leaching of airborne dust particles followed by organomineralization and subsequent precipitation could lead to the formation of mineral bonds between the particles, resulting in their slightly cemented state. However, cementation through bioweathering and mineral precipitation promoted by cyanobacterial activity should not be confused with the weak cementation of loess particles influenced by post-depositional large-scale silicate weathering and precipitation of secondary carbonates, which is one of the main characteristics of loess in arid and semi-arid regions (Pécsi 1990, 1995; Sprafke and Obreht 2016). The main role of biocrusts and, in this case cyanobacteria, is in particle stabilization, preservation and erosion prevention. Cyanobacterial weathering is related to the onset of weak particle alterations followed by EPS mineralization (calcification/silification) and meager carbonate precipitation, enhancing the formation of primary loess structure. In contrast, alteration and weathering of deposited loess on a larger scale is a consequence of increased humidity, the consequential increase in other microbial activity, the development of higher vegetation and consequent increase in humic acids. These processes are related to loessification in the mature phase solely under humid and relatively warm conditions, when deposited loess is strongly influenced by pedogenesis. As a result of those processes, a neo-formation of clays and Fe-oxides occurs, as well as precipitation of carbonate from original horizons and secondary carbonate formation in lower horizons.
The BLOCDUST model proposes that loess formation in arid and semi-arid environments is suppored by BLC and BLM cyanobacterial activity, influenced by environmental shifts between dry and wet events. Stabilization and preservation of the deposited material against wind and water erosion is a central phenomenon in the initial process of loess genesis (Svirčev et al. 2013). The presented scenario may describe not only trapping, deposition and preservation of particles induced by cyanobacteria, but also may shed light on loess granulometry, magnetic properties, thickness, permeability and geographical zonation. From this point of view, loess is not only an eolian sediment (Pécsi 1990; Smalley et al. 2011; Sprafke and Obreht 2016) but is also a biogenic one. Therefore, the processes discussed here should be further assessed in field and laboratory studies to fully understand the bio-geo interactions influencing loess formation. Moreover, it remains to be explored how useful are cyanobacterial biomarkers in assessing this issue and also in paleoclimatic reconstruction, since loess is known as one of the best terrestrial paleoclimate and paleoenvironmental archives (Kukla 1977; Marković et al. 2008; Marković et al. 2011; Pécsi 1990; Pye 1995; Schaetzl et al. 2018; Smalley et al. 2011; Sprafke and Obreht 2016; Stevens et al. 2011; Yang and Ding 2014).
Introduction of a new term: Synergosis
After the presented analysis of the processes and components involved in LPS formation, it is appropriate to give a synthesis of the events leading to loess formation. We propose a new term, synergosis, for a special, sustainable relationship between certain biotic and abiotic constituents located in direct contact and “benefiting” from each other. The following text presents the relationship between BLC and loess as an example of synergosis. The result of this synergotic interaction is stabilized loess. Similar relationships can also be found in some other biogenic formations in nature (soil, stromatolites, travertine, sinter, calcareous nodules and other biogenic rocks) (e.g. Kleinteich et al. 2017; Reid et al. 2000; Riding 2000).
The term synergosis originates from the word synergos (Greek συνεργός), meaning “working together” (from syn- “together” plus ergon “work”). The term synergy originates from the same root, which is defined as the benefit that results when two or more agents work together to achieve something neither one could have achieved on its own (Corning 2005). The suffix -osis denotes a process, condition, state or action.
Synergosis is thus conceived as a bio-abiosis, and is intended to describe the productive efficiency of living and non-living parts of nature when they are “working” together. It represents a close, long-term, productive, sustainable and advantageous interaction between biotic and abiotic components coupled in a physical association. In this sense, the parallel and simultaneous existence of both, BLC and loess deposit, i.e. stabilized loess, is the product of synergosis. The success, or if a more neutral expression is desired, the strength of the synergotic interaction in this particular case, is measured by the systematic stabilization, maintenance and spreading of stabilized loess and the loess environment.
Inspiration for the introduction of the term synergosis was found in the related term “symbiosis”, which defines an interaction between different organisms living in close physical association, usually to the advantage of each of them, or any type of close and long-term biological interaction between two different organisms (Martin and Schwab 2013). In any case, symbiosis, as a qualitatively different creation based on the relationship between its members, refers to living partners. Lichen, as an example of symbiosis, is an association formed by microalgae and/or cyanobacteria and microfungi, each of which receives significant benefits from the association, sometimes so much, that they cannot grow as vegetative forms outside of the symbiosis. In parallel with this example, stabilized loess is a consequence of synergosis between living and inanimate units of nature: BLCs and loess. In principle, any plant communities growing in arid and semi-arid regions may serve as a biocomponent in the described synergosis. A further significant difference between symbiosis and synergosis is that symbiosis typically involves individuals or small communities, while synergosis involves larger-scale (and longer-term) interactions.
Due to the interaction of BLC and loess constituents, a stable (not transient) but growing product, stabilized loess, emerges. Our premise is that BLCs, as the biotic unit, on the surface of loess are actively involved in the accumulation, sedimentation and stabilization of airborne particles (mainly dust) during loess formation, while the abiotic unit (loess and its constituents) at the same time serves as the physical substrate and a source of mineral nutrients for the growth of the BLCs. By working together in this way, BLCs (and/or suitable plants) and windblown dust, later becoming stabilized sedimentary deposits, constitute, sustain and expand the loess environment as final result of the intitial synergotic interaction.
The place of cyanobacterial BLC and BLM in the context of climate change
Loess-paleosol sequences (LPSs) are among the best preserved terrestrial Quaternary archives (Hao et al. 2012; Marković et al. 2011; Muhs 2013; Obreht et al. 2016; Obreht et al. 2019) although their formation in China may have started as early as the Miocene (Guo et al. 2002). The successive layers of loess and paleosol formations evidence past environmental changes, primarily in the past dynamics of dust, vegetation cover and the surface processes they influence. Loess formation is an ongoing process, which currently mostly takes place in warm and arid regions, including in China (Lehmkuhl et al. 2014), Israel (Zaady and Offer 2010) and Iran (Dulić et al. 2017; Kehl 2010). Since rainfall is highly limited in arid and semi-arid regions, dew, fog and humid air are considered potential sources of water in these regions (Kidron et al. 2002; Lange et al. 1992; Maphangwa et al. 2012). Such conditions support the development of dry (semi-desert) steppe vegetation, dominated by different developmental stages of biocrusts (Bowker and Belnap 2008; Rosentreter 1984). Dew has been found to play a role in biocrust activity (Rao et al. 2009a) and can promote the diurnal change between biocrust active and dormant states. Biocrust organisms are also recognized to promote dew formation (Fischer et al. 2012; Liu et al. 2006; Rao et al. 2011). The limited water availability favours the endurance of BLC compared to higher plants during prolonged dry periods and enables rapid development of BLM during intervening short wet periods (e.g. dew). Zaady and Offer (2010) have demonstrated that morning dew is a sufficient moisture source for cyanobacterial biocrusts to trap atmospheric dust. The BLC-BLM change and the reversibility of the process are essential for loess formation (Fig. 4) and may contribute to relatively high accumulation rates of loess during glacial periods.
In the transition from stadials to interstadials, a gradual increase in annual moisture availability would prolong a BLM stage An intensified BLM stage would in turn advance grass species and thus influence the development of successional stages of loess (Fig. 4). Further change towards a warm and humid climate (e.g. changes atglacial to interglacial level) would result in a general vegetation change to the forest-steppe type, characterized by a dense vegetation cover of grass, shrubs and trees. Warm and humid climate conditions and a high biomass content would intensify synsedimentary pedogenesis and the formation of soil horizons. Subsequent soil formation from the Ah-horizon of the chernozem or phaeozem, to the B-horizon of the cambisol or luvisol (Bronger et al. 1998; Bronger 2003) is a consequence of a change from semi-arid to more humid climatic conditions and the significant presence of higher plants (Fig. 4). If the climate changed towards a dryer and colder type, vegetation cover would be reduced and paleosol horizons would be buried by new layers of loess, contributing to the growth of total LPSs.
Environmental and health aspects of cyanobacterial BLC and BLM related to erosion
Throughout semi-arid and arid areas biocrusts stabilize surfaces against wind and water erosion (Belnap 2003b; Belnap et al. 2003b; Eldridge and Leys 2003; Makhalayane et al. 2015; Rodríguez-Caballero et al. 2013). As sediment surface protectors, biocrusts are highly vulnerable to the compressional and shear forces generated by off-road vehicles (e.g. four-wheel drive trucks, all-terrain vehicles and military vehicles), trampling and grazing by livestock and different human activities (Belnap and Eldridge 2003; Belnap et al. 2007; Kovda 1980; Williams et al. 2008). Due to their sensitivity to anthropogenic and natural disturbance, they are in a degraded state in many areas under extensive erosion by wind (Belnap and Gillette 1998; Maestre et al. 2006). The wind and water erosion of (disturbed) biocrusts are thought to lead to a chain reaction as exposed and windblown silt from the substrate has more abrasive force than the wind itself. A disruption in the biocrust may thus lead to that of a larger area. On a regional and long-term scale, land use in loess regions and consequent erosion cause colluviation, while climatic fluctuations are of only secondary importance for colluviation (Lang 2003).
The process of wind erosion of biocrusts may affect human and animal health in two ways. One concern is related to the inhalation of dust induced by the lack of biocrust cover. Loess environments may be hazardous, threatening human occupation, health and livelihood (Derbyshire 2001). North-western China is a major source of windblown dust originating from loess deposits that can adversely affect both human and animal health. The volume of loess being lost from the Chinese Loess Plateau close to Huang He (Yellow River) in a single year is equivalent to the thickness of loess accumulated over 100–300 years (Dai 1987). Written records of the past 500 years suggest that 2–36 dust storms per year occur on or near the Chinese Loess Plateau. Dust storms also influence the quality of life conditions in Beijing, which lies more than 1000 km from the source area (Liu 1985). The effect of such dust upon human health in these extensive loess regions, including many large cities, has still to be fully evaluated, but pneumoconiosis (non-industrial silicosis: NIS) is thought to affect about 24 million people in North-western China (Dai 1987; Derbyshire 2001; Liu 1985; Xu et al. 1993). In one highly exposed village, 45% of a random sample of 150 adults aged 30 and over had the disease (Norboo et al. 1991; Saiyed et al. 1991). Further atmospheric aerosol formation of novel particles has been characterized in China originating from loess dust by condensation, coagulation and photo-induced, surface-mediated reactions (Nie et al. 2014). The toxicology and ecotoxicology of these particles requires investigation.
Another potential health risk in arid and semiarid regions is via the inhalation of wind-blown biocrust particles, which may include cyanobacterial metabolites produced in BLM during the wet- and preserved in BLC during the dry events. Terrestrial and aquatic cyanobacteria can produce a wide range of potent toxins (cyanotoxins) (Metcalf and Codd 2012) of both ecotoxicological and human health relevance. The ecotoxicology of cyanotoxins in terrestrial settings is still poorly known and has to be extrapolated from the more intensively studied production, fates and health significance of these potent cyanobacterial products in aquatic environments. Some of the cyanotoxins, including hepatotoxic microcystins which are inhibitors of the protein phosphatases and phosphoprotein phosphatases of humans, animals and plants, are bound to have adverse effects on practically any eukaryotic organism in any environment provided adequate exposure levels and cellular uptake mechanisms exist (Metcalf and Codd 2012). For humans, the highest risks in the arid and semi-arid environments seem to be associated with the inhalation of toxin-containing cyanobacterial dust and aerosolized cyanotoxins from the biocrusts. Low but toxicologically relevant amounts of microcystins (3 to 56 μg m−2) have been found in desert biocrusts in Qatar (Metcalf et al. 2012). There is also evidence of cyanobacterial neurotoxins in Qatar desert biocrusts. β-N-methylamino-L-alanine (BMAA), produced by aquatic and terrestrial cyanobacteria, is a non-encoded amino acid and suspected environmental risk factor for sporadic amyotrophic lateral sclerosis (ALS) and related human neurodegenerative diseases (Bradley and Cox 2009; Nunn 2017). The BMAA neurotoxin isomers, 2,4-diaminobutyric acid (2,4-DAB) and aminoethylglycine (AEG) also occur and persist in the Qatar cyanobacterial biocrusts (Metcalf et al. 2015; Richer et al. 2015). Anatoxin-a(S), an organophosphate, rapidly-acting cyanobacterial neurotoxin, has also been found in the Qatar cyanobacterial biocrusts and has been linked to lethal poisonings of dogs drinking rainwater from natural depressions on the crust (Chatziefthimiou et al. 2014; Metcalf et al. 2012). Information on the production and fates of cyanotoxins in loess material is lacking, although the high potential for cyanotoxin production by loess cyanobacteria by analogy with aquatic cyanobacteria (Metcalf et al. 2012) and the Qatar biocrust studies (Metcalf et al. 2012, 2015; Richer et al. 2015) motivate the analysis of loess material for cyanotoxins.
The consequences of degrading and removing biocrusts are long lasting and need to be solved by complex restoration processes (Rossi et al. 2017; Zhao et al. 2016). Attempts have been made to establish artificial BSCs to stabilize soil and to reduce losses due to wind and water erosion. For instance, the concept of BSC carpet engineering has been proposed (Wei 2005). Restoration of exposed loess surfaces has been a great challenge in recent decades. Moss-dominated BLC have already been tested as a means to mitigate extensive loess erosion. While laboratory results were promising (Xiao et al. 2011; Zhao et al. 2014a), the successful implementation of field applications has differed significantly (Xiao et al. 2015), so the problem persists. For land restoration, much interest has been focused on the effects of cyanobacterial inoculation in arid and semiarid regions (Acea et al. 2001; Belnap 1993; Bu et al. 2015; De Caire et al. 2000; Hu et al. 2002a; Lan et al. 2014; Nisha et al. 2007; Rao et al. 2009b; Rossi et al. 2017; Tiedemann et al. 1980; Wang et al. 2009). Since the moss-dominated biocrusts are the last development stage of biocrusts and require a preceding adaptation of the habitat (Belnap 2003c), the restoration of exposed loess surfaces should be addressed with pioneering cyanobacterial species. Nonetheless, while producing artificial cyanobacterial biocrusts by inoculation and spraying in the field are feasible, their persistence in the field is still a future challenge (Bu et al. 2013; Rossi et al. 2015).
This paper has summarized the wide-scale occurrence of cyanobacteria in biocrusts and the integral role of cyanobacteria in the formation of loess as envisaged via the BLOCDUST hypothesis. Emerging concepts and arising needs include:
Synergosis: a new term proposed here to describe large-scale biotic - abiotic interactions of a specific type. Stabilized loess would not develop without this beneficial interaction: the constituents of loess serve as a nutrient source for the organisms of BLCs, while BLC organisms bind and preserve dust in the form of loess. By working together in this way, BLCs and loess constituents form, sustain and expand stabilized loess as the result of synergosis.
The role of cyanobacteria in loess formation (loessification) has only recently been recognized, and the possible biogenic nature of loessification is underestimated as compared to its eolian nature.
The BLOCDUST hypothesis of cyanobacteria-promoted loessification needs to be tested in laboratory and field experiments to justify a potential theory for the eolian-biogenic formation of loess.
With reference to cyanotoxin production, the significance of terrestrial cyanobacteria to human health is poorly understood compared to that of aquatic cyanobacteria. Information is needed on the cyanotoxin content of BLCto permit adequate human health risk assessment of airborne exposure to loess-derived particles. Inhalation of biocrust/dust particles caused by erosion can be considered as a potential health hazard.
The practice of using cyanobacterial crusts for the stabilization and restoration of exposed substrates is still a developing field.
biological loess crust
biological loess mat
biological soil crust
biological desert crust
Acea MJ, Diz N, Prieto-Fernandez A (2001) Microbial populations in heated soils inoculated with cyanobacteria. Biol Fertil Soils 33:118–125
Acea MJ, Prieto-Fernández A, Diz-Cid N (2003) Cyanobacterial inoculation of heated soils: effect on microorganisms of C and N cycles and on chemical composition in soil surface. Soil Biol Biochem 35:513–524
Belnap J (1993) Recovery rates of cryptobiotic crusts: inoculant use and assessment methods. Great Bas Nat 53:89–95
Belnap J (1995) Surface disturbances: their role in accelerating desertification. Environ Monit Assess 37:39–57
Belnap J (2001) Comparative structure of physical and biological soil crusts. In: Belnap J, Lange OL (eds), Biological soil crusts: structure, function, and management.Springer-Verlag ,Berlin, pp177–191
Belnap J (2003a) Microbes and microfauna associated with biological soil crusts. In: Belnap J, Lange OL (eds), Biological soil crusts: structure, function, and management. Springer-Verlag, Berlin ,pp167–174
Belnap J (2003b) Biological soil crusts and wind erosion. In: Belnap J, Lange OL (eds), Biological soil crusts: structure, function, and management. Springer-Verlag, Berlin, pp339–347
Belnap J (2003c) The world at your feet: desert biological soil crusts. Front Ecol Environ 1:181–189
Belnap J (2006) The potential roles of biological soil crusts in dryland hydrologic cycles. Hydrol Process 20:3159–3178
Belnap J, Eldridge D (2003) Disturbance and recovery of biological soil crusts. In: Belnap J, Lange OL (eds) Biological soil crusts: structure, function, and management. Springer-Verlag, Berlin, pp 363–383
Belnap J, Gardner JS (1993) Soil microstructure in soils of the Colorado plateau: the role of the cyanobacterium Microcoleus vaginatus. Great Bas Nat 53:40–47
Belnap J, Gillette DA (1998) Vulnerability of desert biological soil crusts to wind erosion: the influences of crust development, soil texture, and disturbance. J Arid Environ 39:133–142
Belnap J, Lange OL (2003) Biological soil crusts: structure, function, and management. Springer-Verlag, Berlin
Belnap J, Büdel B, Lange OL (2003a) Biological soil crusts: characteristics and distribution. In: Belnap J, Lange OL (eds), Biological soil crusts: structure, function, and management. Springer-Verlag, Berlin, pp 3–30
Belnap J, Hawkes CV, Firestone MK (2003b) Boundaries in miniature: two examples from soil. BioScience 53:739–749
Belnap J, Phillips SL, Herrick JE, Johansen JR (2007) Wind erodibility of soils at Fort Irwin, California (Mojave Desert), USA, before and after trampling disturbance: implications for land management. Earth Surf Process Landf 32:75–84
Berkeley A, Thomas AD, Dougill AJ (2005) Spatial dynamics of biological soil crusts: bush canopies, litter and burial in Kalahari rangelands. Afr J Ecol 43:137–145
Billi D, Potts M (2002) Life and death of dried prokaryotes. Res Microbiol 153:7–12
Bowker MA, Belnap J (2008) A simple classification of soil types as habitats of biological soil crusts on the Colorado plateau, USA. J Veg Sci 19:831–840
Braccini I, Grasso RP, Pérez S (1999) Conformational and configurational features of acidic polysaccharides and their interactions with calcium ions: a molecular modelling investigation. Carbohydr Res 317(1–4):119–130
Bradley WG, Cox PA (2009) Beyond Guam: cyanobacteria, BMAA and sporadic amyotrophic lateral sclerosis. Amyotroph Lateral Scler 10:5–6
Braissant O, Cailleau G, Dupraz C, Verrecchia EP (2003) Bacterially induced mineralization of calcium carbonate in terrestrial tnvironments: the role of exopolysaccharides and amino acids. J Sediment Res 73(3):485–490
Bronger A (2003) Correlation of loess-paleosol sequences in East and Central Asia with SE Central Europe - towards a continental quaternary pedostratigraphy and paleoclimatic history. Quat Int 106-107:11–31
Bronger A, Winter R, Sedov S (1998) Weathering and clay mineral formation in two Holocene soils and in buried paleosols in Tajikistan towards a quaternary paleoclimatic record in Central Asia. Catena 34:19–34
Bu CF, Wu SF, Xie YS, Zhang XC (2013) The study of biological soil crusts: hotspots and prospects. Clean 41:899–906
Bu CF, Wu SF, Zhang KK, Yang YS, Gao GX (2015) Biological soil crusts: an Eeo-adaptive biological conservative mechanism and implications for ecological restoration. Plant Biosyst 149:364–373
Büdel B, Weber B, Kühl M, Pfanz H, Sültemeyer D, Wessels D (2004) Reshaping of sandstone surfaces by cryptoendolithic cyanobacteria: bioalkalization causes chemical weathering in arid landscapes. Geobiology 2:261–268
Buis E, Veldkamp A, Boeken B, van Breemen N (2009) Controls on plant functional surface cover types along a precipitation gradient in the Negev Desert of Israel. J Arid Environ 73:82–90
Chamizo S, Cantón Y, Miralles I, Domingo F (2012) Biological soil crust development affects physicochemical characteristics of soil surface in semiarid ecosystems. Soil Biol Biochem 49:96–105
Chamizo S, Mugnai G, Rossi F, Certini G, De Philippis R (2018) Cyanobacterial inoculation improves soil stability and fertility on different textured soils: gaining insights for applicability in soil restoration. Front Environ Sci 6:49
Chatziefthimiou AD, Richer R, Roles H, Powell JT, Metcalf JS (2014) Cyanotoxins as a potential cause of dog poisonings in desert environments. Vet Rec 174:484–485
Cockell CS, Knowland J (1999) Ultraviolet radiation screening compounds. Biol Rev 74:311–345
Colesie C, Felde VJMNL, Büdel B (2016) Composition and macrostructure of biological soil crusts. In: Weber B, Büdel B, Belnap J (eds) Biological soil crusts: an organizing principle in drylands. Springer Nature, Switzerland, pp 159–172
Corning P (2005) Holistic Darwinism: synergy, cybernetics, and the bioeconomics of evolution. The University of Chicago Press Books, Chicago
Dai YS (1987) The engineering geological characteristics of the loess and soil erosion in the middle reaches of the Huanghe River. In: Liu TS (ed) Aspects of loess research. China Ocean Press, Beijing, pp 432–436
Danin A (1983) Weathering of limestone in Jerusalem by cyanobacteria. Z Geomorphol 27(4):413–421
Danin A, Ganor E (1991) Trapping of airborne dust by mosses in the Negev Desert, Israel. Earth Surf Proc Land 16:153–162
De Caire GZ, De Cano MS, Palma RM, De Mule CZ (2000) Changes in soil enzyme activities following additions of cyanobacterial biomass and exopolysaccharide. Soil Biol Biochem 32:1985–1987
Derbyshire E (2001) Geological hazards in loess terrain, with particular reference to the loess regions of China. Earth Sci Rev 54:231–260
Dougill AJ, Thomas AD (2004) Kalahari sand soils: spatial heterogeneity, biological soil crusts and land degradation. Land Degrad Dev 15:233–242
Dulić T, Meriluoto J, Palanački Malešević T, Gajić V, Važić T, Tokodi N, Obreht I, Kostić B, Kosijer P, Khormali F, Svirčev Z (2017) Cyanobacterial diversity and toxicity of biocrusts from the Caspian lowland loess deposits. North Iran Quat Int 429:74–85
Dupraz C, Reid PR, Braissant O, Decho AW, Norman SR, Visscher PT (2009) Processes of carbonate precipitation in modern microbial mats. Earth Sci Rev 96:141–162
Eldridge DJ, Leys JF (2003) Exploring some relationships between biological soil crusts, soil aggregation and wind erosion. J Arid Environ 53:457–466
Evans RD, Johansen JR (1999) Microbiotic crusts and ecosystem processes. CRC Crit Rev Plant Sci 18:183–225
Felde VJMNL, Chamizo S, Felix-Henningsen P, Drahorad SL (2017) What stabilizes biological soil crusts in the Negev Desert? Plant Soil 429:9–18
Fischer T, Veste M, Bens O, Hüttl RF (2012) Dew formation on the surface of biological soil crusts in central European sand ecosystems. Biogeosciences 9:4621–4628
Gallagher KL, Dupraz C, Braissant O, Norman RS, Decho AW, Visscher PT (2010) Mineralization of sedimentary biofilms: modern mechanistic insights. In: Bailey WC (ed) Biofilms: formation. Development and Properties. Nova Science Publishers, Inc, New York, pp 227–258
Garcia-Pichel F (2006) Plausible mechanisms for the boring on carbonates by microbial phototrophs. Sediment Geol 185:205–213
Garcia-Pichel F, Belnap J (1996) Microenvironments and microscale productivity of cyanobacterial desert crusts. J Phycol 32:774–782
Garcia-Pichel F, Castenholz RW (1991) Characterization and biological implications of scytonemin, a cyanobacterial sheath pigment1. J Phycol 27:395–409
Garcia-Pichel F, Castenholz RW (1993) Occurrence of UV-absorbing, mycosporine-like compounds among cyanobacterial isolates and an estimate of their screening capacity. Appl Environ Microbiol 59:163–169
Garcia-Pichel F, Ramírez-Reinat E, Gao Q (2010) Microbial excavation of solid carbonates powered by P-type ATPase-mediated transcellular Ca2+ transport. PNAS 107:21749–21754
Garcia-Pichel F, Felde VJMNL, Drahorad SL, Weber B (2016) Microstructure and weathering processes within biological soil crusts. In: Weber B, Büdel B, Belnap J (eds) Biological soil crusts: an organizing principle in drylands. Springer Nature, Switzerland, pp 237–255
Gorbushina AA (2007) Life on the r ocks. Environ Microbiol 9:1613–1631
Goudie AS, Viles HA (2012) Weathering and the global carbon cycle: geomorphological perspectives. Earth Sci Rev 113:59–71
Guo ZT, Ruddiman WF, Hao QZ, Wu HB, Qiao YS, Zhu RX, Peng SZ, Wei JJ, Yuan BY, Liu TS (2002) Onset of Asian desertification by 22 Myr ago inferred from loess deposits in China. Nature 416:159–163
Hao Q, Wang L, Oldfield F, Peng S, Qin L, Song Y, Xu QY, Bloemendal J, Guo Z (2012) Delayed build-up of Arctic ice sheets during 400,000-year minima in insolation variability. Nature 490:393–396
Hershkovitz N, Ohren A, Cohen Y (1991) Accumulation of trehalose and sucrose in cyanobacteria exposed to matric water stress. Appl Environ Microbiol 57:645–648
Hu CX, Liu YD (2003) Primary succession of algal community structure in desert soil. Acta Bot Sin 45:917–924
Hu C, Liu Y, Song L, Zhang D (2002a) Effect of desert soil algae on the stabilization of fine sands. J Appl Phycol 14:281–292
Hu C, Liu Y, Zhang D, Huang Z, Paulsen BS (2002b) Cementing mechanism of algal crusts from desert area. Chin Sci Bull 46:1361–1368
Karnieli A, Gabai A, Ichoku C, Zaady E, Shachak M (2002) Temporal dynamics of soil and vegetation spectral responses in a semi-arid environment. Int J Remote Sens 23:4073–4087
Kehl M (2010) Quaternary Loesses, loess-like sediments, soils and climate change in Iran. Relief Boden Palaeoklima, band 24. Borntraeger Science Publishers, Stuttgart
Kidron GJ, Herrnstadt I, Barzilay E (2002) The role of dew as a moisture source for sand microbiotic crusts in the Negev Desert, Israel. J Arid Environ 52:517–533
Kidron GJ, Vonshak A, Dor I, Barinova S, Abeliovich A (2010) Properties and spatial distribution of microbiotic crusts in the Negev Desert, Israel. Catena 82:92–101
Kleinteich J, Golubic S, Pessi IS, Velázquez D, Storme JY, Darchambeau F, Borges AV, Compère P, Radtke G, Lee SJ, Javaux EJ, Wilmotte A (2017) Cyanobacterial contribution to travertine deposition in the Hoyoux River system, Belgium. Microb Ecol 74:33–53
Kovda V (1980) Land Aridization and drought control. Westview Press, Boulder
Kukla GJ (1977) Pleistocene land-sea correlations I. Europe. Earth Sci Rev 13:307–374
Kurina LM, Vitousek PM (1999) Controls over the accumulation and decline of a nitrogen-fixing lichen, Stereocaulon vulcani, on young Hawaiian lava flows. J Ecol 87:784–799
Lan S, Wu L, Zhang D, Hu C (2012) Successional stages of biological soil crusts and their microstructure variability in Shapotou region (China). Environ Earth Sci 65:77–88
Lan SB, Wu L, Zhang DL, Hu CX (2013) Assessing level of development and successional stages in biological soil crusts with biological indicators. Microb Ecol 66:394–403
Lan S, Zhang Q, Wu L, Liu Y, Zhang D, Hu C (2014) Artificially accelerating the reversal of desertification: cyanobacterial inoculation facilitates the succession of vegetation communities. Environ Sci Technol 48:307–315
Lang A (2003) Phases of soil erosion-derived colluviation in the loess hills of South Germany. Catena 51:209–221
Lange OL, Kidron EL, Büdel B, Meyer A, Kilian E, Abeliovich A (1992) Taxonomic composition and photosynthetic characteristics of the ‘biological soil crusts’ covering sand dunes in the western Negev Desert. Funct Ecol 6:519–527
Lange OL, Belnap J, Reichenberger H, Meyer A (1997) Photosynthesis of green algal soil-crust lichens from arid lands in southern Utah, USA—role of water content on light and temperature responses of CO2 exchange. Flora 192:1–15
Langhans TM, Storm C, Schwabe A (2009) Community assembly of biological soil crusts of different successional stages in a temperate sand ecosystem, as assessed by direct determination and enrichment techniques. Microb Ecol 58:394–407
Langhans TM, Storm C, Schwabe A (2010) Regeneration processes of biological soil crusts, macro-cryptogams and vascular plants species after fine-scale disturbance in a temperate region: recolonization or successional replacement? Flora 205:46–60
Lehmkuhl F, Schulte P, Zhao H, Hülle D, Protze J, Stauch G (2014) Timing and spatial distribution of loess and loess-like sediments in the mountain areas of the northeastern Tibetan Plateau. Catena 117:23–33
Liu TS (1985) Loess and the environment. Science Press, Beijing
Liu LC, Li SZ, Duan ZH, Wang T, Zhang ZS, Li XR (2006) Effects of microbiotic crusts on dew deposition in the restored vegetation area at Shapotou, northwestern China. J Hydrol 328:331–337
Lukešová A (2001) Soil algae in brown coal and lignite post-mining areas in Central Europe (Czech Republic and Germany). Restor Ecol 9:341–350
Maestre FT, Martín N, Beatriz Díez B, López-Poma R, Santos F, Luque I, Cortina J (2006) Watering, fertilization, and slurry inoculation promote recovery of biological crust function in degraded soils. Microb Ecol 52:365–377
Makhalayane TP, Valverde A, Gunnigle E, Frossard A, Ramond J-P, Cowan DA (2015) Microbial ecology of hot desert edaphic systems. FEMS Microb Ecol 39:203–221
Malam Issa O, Trichet J, Défarge C, Valentin C (1999) Morphology and microstructure of microbiotic soil crusts on a tiger bush sequence (Niger, Sahel). Catena 37:175–196
Malam Issa O, Le Bissonnais Y, Défarge C, Trichet J (2001) Role of a cyanobacterial cover on structural stability of sandy soils in the Sahelian part of western Niger. Geoderma 101:15–30
Maphangwa KW, Musil CF, Raitt L, Zedda L (2012) Differential interception and evaporation of fog, dew and water vapour and elemental accumulation by lichens explain their relative abundance in a coastal desert. J Arid Environ 82:71–80
Marković SB, Bokhorst M, Vandenberghe J, Oches EA, Zöller L, McCoy WD, Gaudenyi T, Jovanović M, Hambach U, Machalett B (2008) Late Pleistocene loess-paleosol sequences in the Vojvodina region, North Serbia. J Quat Sci 23:73–84
Marković SB, Hambach U, Stevens T, Kukla GJ, Heller F, McCoy WD, Oches EA, Buggle B, Zöller L (2011) The last million years recorded at the Stari Slankamen loess-palaeosol sequence: revised chronostratigraphy and long term environmental trends. Quat Sci Rev 30:1142–1154
Martin BD, Schwab E (2013) Current usage of symbiosis and associated terminology. Int J Biol 5:32–45
McKenna Neuman C, Maxwell CD, Boulton JW (1996) Wind transport of sand surfaces crusted with photoautotrophic microorganisms. Catena 27:229–247
Metcalf JS, Codd GA (2012) Cyanotoxins. In: Whitton BA (ed) Ecology of cyanobacteria II: their diversity in space and time. Springer Science & Business Media, Dordrecht, pp 651–675
Metcalf JS, Richer R, Cox PA, Codd GA (2012) Cyanotoxins in desert environments may present a risk to human health. Sci Total Environ 421-422:118–123
Metcalf JS, Banack SA, Richer R, Cox PA (2015) Neurotoxic amino acids and their isomers in desert environments. J Arid Environ 112:140–144
Muhs D (2007) Loess deposits, origins and properties. In: Elias SA (ed) Encyclopedia of Quaternary Science. Elsevier Ltd, Oxford, pp 1405–1418
Muhs DR (2013) The geologic records of dust in the quaternary. Aeol Res 9:3–48
Muhs DR, Bettis EA III (2003) Quaternary loess-paleosol sequences as examples of climate-driven sedimentary extremes. Geol Soc Spec Pap 370:53–74. https://doi.org/10.1130/0-8137-2370-1.53
Nie W, Ding A, Wang T, Kerminen VM, George C, Xue L, Wang W, Zhang Q, Petäjä T, Qi X, Gao X, Wang X, Yang X, Fu C, Kulmala M (2014) Polluted dust promotes new particle formation and growth. Sci Rep 4:6634
Nisha R, Kaushik A, Kaushik CP (2007) Effect of indigenous cyanobacterial application on structural stability and productivity of an organically poor semiarid soil. Geoderma 138:49–56
Norboo T, Angchuk PT, Yahya M (1991) Silicosis in a Himalayan village population: role of environmental dust. Thorax 46:341–343
Nunn PB (2017) 50 years of research on α-amino-β-methylaminopropionic acid (β-methylaminoalanine). Phyochemistry 144:271–281
Obreht I, Zeeden C, Hambach U, Veres D, Marković SB, Bösken J, Svirčev Z, Bačević N, Gavrilov MB, Lehmkuhl F (2016) Tracing the influence of Mediterranean climate on Southeastern Europe during the past 350,000 years. Sci Rep 6:36334
Obreht I, Zeeden C, Hambach U, Veres D, Marković SB, Lehmkuhl F (2019) A critical reevaluation of palaeoclimate proxy records from loess in the Carpathian Basin. Earth Sci Rev 190:498–520
Pécsi M (1990) Loess is not just the accumulation of dust. Quat Int 7:1–21
Pécsi M (1995) The role of principles and methods in loess-paleosol investigations. GeoJournal 36:117–131
Pickett STA, McDonnell MJ (1989) Changing perspectives in community dynamics: a theory of successional forces. Trends Ecol Evol 4:241–245
Pietrasiak N, Drenovsky RE, Santiago LS, Graham RC (2014) Biogeomorphology of a Mojave Desert landscape – configurations and feedbacks of abiotic and biotic land surfaces during landform evolution. Geomorphology 206:23–36
Pócs T (2009) Cyanobacterial crust types, as strategies for survival in extreme habitats. Acta Bot Hung 51:147–178
Pócs T, Gánti T, Horváth A, Bérczis Z, Kereszturi A, Sik A, Szathmáry E (2006) Comparison of the cryptobiotic-crusts and surface mineral crusts according to their main characteristics in helping life support mechanisms and their implied role for Martian living organisms. In:Proceedings of the 30th Conference on Antarctic Meteorites,June 6–8. National Institute of Polar Research,Tokyo, pp 99–100
Potts M (1994) Desiccation tolerance of prokaryotes. Microbiol Rev 58:755–805
Pye K (1995) The nature, origin and accumulation of loess. Quat Sci Rev 14:653–667
Ramírez-Reinat EL, Garcia-Pichel F (2012) Prevalence of Ca2+-ATPase-mediated carbonate dissolution among cyanobacterial euendoliths. Appl Environ Microbiol 78:7–13
Rao B, Liu Y, Wang W, Hu C, Dunhai L, Lan S (2009a) Influence of dew on biomass and photosystem II activity of cyanobacterial crusts in the Hopq Desert, Northwest China. Soil Biol Biochem 41:2387–2393
Rao BQ, Liu YD, Hu CX, Li DH, Shen YW (2009b) The technology of manmade algal crust and its applications in control of desertification. Acta Hydrobiol Sin 33:756–761
Rao BQ, Wu YW, Li H, Li DH, Liu YD (2011) Comparison studies on dew condensation of different developmental artificial crusts in Hopq Desert. J Soil Water Conserv 25:159–164
Rastogi RP, Sonani RR, Madawar D (2014) The high-energy radiation protectant extracellular sheath pigment scytonemin and its reduced equivalent in the cyanobacterium Scytonema sp. R77DM. Bioresour Technol 171:396–400
Reid RP, Visscher PT, Decho AW, Stolz JF, Bebout BM, Dupraz C, Macintyre IG, Paerl HW, Pinckney HL, Prufert-Bebout L, Stepper TF, MesMarais DJ (2000) The role of microbes in accretion, lamination and early lithification of modern marine stromatolites. Nature 406:989–992
Richer R, Banack SA, Metcalf JS, Cox PA (2015) The persistence of cyanobacterial toxins in desert soils. J Arid Environ 112:134–139
Riding R (2000) Microbial carbonates: the geological record of calcified bacterial–algal mats and biofilms. Sedimentology 47:179–214
Rodríguez-Caballero E, Canton Y, Chamizo S, Lazaro R, Escudero A (2013) Soil loss and runoff in semiarid ecosystems: a complex interaction between biological soil crusts, micro-topography, and hydrological drivers. Ecosystems 16:529–546
Rosentreter R (1984) Compositional patterns within a rabbitbrush (Chrysothamnus) community of the Idaho Snake River plain. In: proceedings, symposium on the biology of Artemisia and Chrysothamnus. US Department of Agriculture General Technical Report, INT-200, pp 273–277
Rossi F, De Philippis R (2015) Role of cyanobacterial exopolysaccharides in phototrophic biofilms and in complex microbial mats. Life 5:1218–1238
Rossi F, Olguín EJ, Diels L, De Philippis R (2015) Microbial fixation of CO2 in water bodies and in drylands to combat climate change, soil loss and desertification. New Biotechnol 32:109–120
Rossi F, Lib H, Liub Y, De Philippis R (2017) Cyanobacterial inoculation (cyanobacterisation): perspectives for the development of a standardized multifunctional technology for soil fertilization and desertification reversal. Earth Sci Rev 171:28–43
Rubin M, Berman-Frank I, Shaked Y (2011) Dust- and mineral-iron utilization by the marine dinitrogen-fixer Trichodesmium. Nat Geosci 4:529–534
Saiyed HN, Sharma YK, Sadhus HG (1991) Non-occupational pneumoconiosis at high altitude villages in Central Ladakh. Br J Ind Med 48:825–829
Schaetzl R, Bettis EA, Crouvi O, Fitzsimmons KE, Grimley DA, Hambach U, Lehmkuhl F, Marković SB, Mason JA, Owczarek P, Roberts HM, Rousseau D-D, Stevens T, Vandenberghe J, Zárate M, Veres D, Yang S, Zech M, Conroy JL, Dave AK, Faust D, Hao Q, Obreht I, Prud'homme C, Smalley I, Tripaldi A, Zeeden C, Zech R (2018) Approaches and challenges to the study of loess - introduction to the LoessFest special issue. Quat Res 89:563–618
Shirkey B, Kovarcik DP, Wtight DJ, Wilmoth G, Prickett TF, Helm RF, Gregory EM, Potts M (2000) Active Fe-containing superoxide dismutase and abundant sodF mRNA in Nostoc commune (Cyanobacteria) after years of desiccation. J Bacteriol 182:189–197
Smalley IJ, Marković SB (2014) Loessification and hydroconsolidation: there is a connection. Catena 117:94–99
Smalley IJ, Jefferson IF, O’Hara-Dhand K, Evand RD (2006) An approach to the problem of loess deposit formation: some comments on the ‘in situ’ or ‘soil-eluvial’ hypothesis. Quat Int 152:109–117
Smalley IJ, Marković SB, Svirčev Z (2011) Loess is [almost totally formed by] the accumulation of dust. Quat Int 240:4–11
Sprafke T, Obreht I (2016) Loess: rock, sediment or soil - what is missing for its definition? Quat Int 399:198–207
Stevens T, Marković SB, Zech M, Hambach U, Sümegi P (2011) Dust deposition and climate in the Carpathian Basin over an independently dated last glacial-interglacial cycle. Quat Sci Rev 30:662–681
Svirčev Z, Marković SB, Stevens T, Codd GA, Simeunovć J, Obreht I, Dulić T, Pantelić D, Hambach U (2013) Importance of biological loess crusts for loess formation in semi-arid environments. Quat Int 296:206–215
Thomas AD, Dougill AJ (2007) Spatial and temporal distribution of cyanobacterial soil crusts in the Kalahari: implications for soil surface properties. Geomorphology 85:17–29
Tiedemann AR, Lopushinsky W, Larsen HJ Jr (1980) Plant and soil responses to a commercial blue–green algae inoculant. Soil Biol and Biochem 12:471–475
Trichet J, Défarge C (1995) Non-biologically supported organomineralization. Bull Inst Océanogr Monaco 14:203–236
Verrecchia EP, Freytet P, Verrecchia KE, Dumont J-L (1995) Spherulites in calcrete laminar crusts: biogenic CaCO3 precipitation as a major contributor to crust formation. J Sedim Res 65:690–700
Viles H (1995) Ecological perspectives on rock surface weathering: towards a conceptual model. Geomorphology 13:21–35
Wang WB, Liu YD, Li DH, Hu CX, Rao BQ (2009) Feasibility of cyanobacteria inoculation for biological soil crusts formation in desert area. Soil Biol Biochem 41:926–929
Weber B, Büdel B, Belnap J (2016) Biological Soild crusts: an organizing principle in drylands. Springer International Publishing, Switzerland
Wei JC (2005) Biocarpet engineering using microbiotic crust for controlling sand. Arid Zone Research (in Chinese) 22:287–288
West NE (1990) Structure and function of microphytic soil crusts in wild land ecosystems of arid to semi-arid regions. Adv Ecol Res 20:179–223
Whitelam GC, Codd GA (1986) Damaging effects of light on microorganisms. Spec Pub Soc Gen Microbiol 17:129–169
Williams JW, Eldridge JD, Alchin MB (2008) Grazing and drought reduce cyanobacterialsoil crusts in an Australian acacia woodland. J Arid Environ 72:1064–1075
Williams AJ, Buck BJ, Beyene MA (2012) Biological soil crusts in the Mojave Desert, USA: micromorphology and pedogenesis. Soil Sci Soc Am J 76:1685–1695
Williams AJ, Buck BJ, Soukup DA, Douglas MJ (2013) Geomorphic controls on biological soil crust distribution: a conceptual model from the Mohave Desert (USA). Geomorphology 195:99–109
Wolff-Boenisch D, Gislason SR, Oelkers EH (2006) The effect of crystallinity on dissolution rates and CO2consumption capacity of silicates. Geochim Cosmochim Acta 70:858–870
Xiao B, Wang QH, Zhao YG, Shao MA (2011) Artificial culture of biological soil crusts and its effects on overland flow and infiltration under simulated rainfall. Appl Soil Ecol 48:11–17
Xiao B, Zhao Y, Wang B, Li C (2015) Development of artificial moss-dominated biological soil crusts and their effects on runoff and soil water content in a semi-arid environment. J Arid Environ 117:75–83
Xie Z, Liu Y, Hu C, Chen L, Li D (2007) Relationships between the biomass of algal crusts in fields and their compressive strength. Soil Biol Biochem 39:567–572
Xu XZ, Cai XG, Men XS (1993) A study of siliceous pneumoconiosis in a desert area of Sunan County, Gansu province, China. Biomed Environ Sci 6:217–222
Yang S, Ding Z (2014) A 249 Kyr stack of eight loess grain size records from northern China documenting millennial-scale climate variability. Geochem Geophy Geosy 15:798–814
Zaady E, Offer ZY (2010) Biogenic soil crusts and soil depth: a long-term case study from the Central Negev desert highland. Sedimentology 57:351–358
Zaady E, Kuhn U, Wilske B, Sandoval-Soto L, Kesselmeier J (2000) Patterns of CO2 exchange in biological soil crusts of successional age. Soil Biol Biochem 32:959–966
Zhang YM (2005) The microstructure and formation of biological soil crusts in their early development stage. Chin Sci Bull 50(2):117–121
Zhang BC, Zhou XB, Zhang YM (2015) Responses of microbial activities and soil physico-chemical properties to the successional process of biological soil crusts in the Gurbantunggut Desert, Xinjiang. J Arid Land 7:101–109
Zhao Y, Zhu Q, Li P, Zhao L, Wang L, Zheng X, Ma H (2014a) Effects of artificially cultivated biological soil crusts on soil nutrients and biological activities in the loess plateau. J Arid Land 6:742–752
Zhao Y, Quin N, Webber B, Xu M (2014b) Response of biological soil crusts to raindrop erosivity and underlying influences in the hilly loess plateau region, China. Biodivers Conserv 23(7):1669–1686
Zhao Y, Bowker MA, Zhang Y, Zaady E (2016) Enhanced recovery of biological soil crusts after disturbance. In: Weber B, Büdel B, Belnap J (eds) Biological soil crusts: an organizing principle in drylands. Springer International Publishing, Cham, pp 499–523
ZS and SBM acknowledge the support of the Ministry of Education, Science and Technological Development of the Serbian Government (project number: 176020). ZS and JM thank the Oskar Öflund Foundation (Finland) for funding for BLC research. TD was supported by a grant from the Erasmus Mundus EUROWEB+ Scholarship Programme and an Åbo Akademi University doctoral research grant. Preparation of this publication was partly performed within the framework of the ERASMUS+ mobility program established between the University of Novi Sad Faculty of Sciences and Åbo Akademi University, Project Code 2017-1-FI01-KA107-034440.
Open access funding provided by Åbo Akademi University (ABO).
Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
Responsible Editor: Alexia Stokes.
Electronic supplementary material
About this article
Cite this article
Svirčev, Z., Dulić, T., Obreht, I. et al. Cyanobacteria and loess—an underestimated interaction. Plant Soil 439, 293–308 (2019). https://doi.org/10.1007/s11104-019-04048-3