The Relative Importance of Cell Wall and Lumen Phytoliths in Carbon Sequestration in Soil: A Hypothesis

Introduction

The sequestration of carbon in soils has now become a topic of global significance. It is recognized that soils store very considerable amounts of carbon. If we could find ways of increasing that storage it might go some way toward stabilizing atmospheric carbon dioxide concentrations and thereby help in the fight against climate change. Powlson et al. (2011) pointed out that carbon sequestration in soil suffered from a number of constraints. Firstly, the quantity of carbon stored is finite. Secondly, the process is reversible. Finally soil organic carbon may be increased, but there may be changes in the fluxes of nitrous oxide and methane, important greenhouse gasses.

Parr and Sullivan (2005) first suggested the possibility that phytoliths could play a major part in carbon sequestration in soils. Their proposition was that so-called phytolith occluded carbon (PhytOC) might be locked up in phytoliths for centuries or longer, and not be returned to the atmosphere as quickly as other components of the soil organic matter. So the idea is that carbon sequestered as PhytOC would be less labile, and the reversible nature of sequestration mentioned by Powlson et al. (2011) would be reduced. In their abstract Parr and Sullivan wrote, “Estimated PhytOC accumulation rates were between 15 and 37% of the estimated global mean long-term (i.e., on a millennial scale) soil carbon accumulation rate of 2.4 g C m⁻² year⁻¹ indicating that the accumulation of PhytOC within soil is an important process in the terrestrial sequestration of carbon.” If true, this would be a highly significant finding that could have very major implications for our understanding of the global carbon cycle and for methodologies to reduce global warming. Parr and Sullivan also suggested that it might be possible to select plant species that were particularly high in PhytOC to increase carbon sequestration. Their work stimulated the interest of researchers around the world, and there are now many publications on this topic. However, work on PhytOC has not been without controversy. As, we shall see below this has focused on methodology, with different methods of preparing phytoliths for analysis giving different values for PhytOC. Essentially, if a technique gives a high value for PhytOC then when the value is entered into the equations for estimating global carbon sequestration it will suggest that phytoliths are very important in this process. Conversely, if PhytOC values measured are low then the calculated sequestration at a global scale will be low. This has led to a vigorous debate: what is the “real” value of PhytOC? A related, and even more disputed, area of phytolith research at the moment is the whole topic of “old carbon” from the soil being taken up by plants, and deposited in phytoliths, causing problems in carbon dating. I have covered this area in two recent reviews (Hodson, 2016, 2018) and do not intend to look at it again here.

Phytoliths are morphologically diverse (Madella et al., 2005; Piperno, 2006), but it is becoming increasingly evident that they are also chemically diverse (Hodson, 2016). Kumar et al. (2017b) reviewed the various locations where phytoliths were found in grasses. It appears that silica deposition occurs in all tissues, including the roots, stems, leaves, inflorescence and seed (caryopsis), but that it is concentrated in certain organs and tissues. In the roots, silica is deposited in the endodermis, in the stems, leaves and inflorescence bracts the main deposition sites are in the epidermis, and small amounts are deposited in the seed in brush hairs and other locations. Less work has been done on species other than grasses and cereals, but in general the epidermis in leaves is the major location for most silica deposition (Piperno, 2006). There are three main types of silica deposition in plants: that where silica is deposited onto a carbohydrate matrix such as the cell wall; that where silica deposition lacks an obvious matrix onto which it is deposited, mainly in the cell lumen; and in intercellular spaces (Hodson, 2016). It does not appear that deposition in intercellular spaces is important in the production of recognizable phytoliths that survive once the plant dies, and so the two main types we need to consider are those in the cell walls and the cell lumen. I have previously assessed the evidence that the cell wall and lumen phytoliths have very different chemistries (Hodson, 2016, 2018). Here, we will concentrate on carbon within phytoliths. It would be expected that higher carbon concentrations will be found in cell wall types that are deposited on a carbohydrate matrix, and the evidence available suggests that this is the case.

There has been very little consideration of which phytolith types are the most important for PhytOC and carbon sequestration. This is, perhaps, surprising given the interest in this topic. The aim of this paper will be to bring together the available literature and to assess the relative importance of cell wall and lumen phytoliths in carbon sequestration. I will then develop a hypothesis concerning what happens to phytoliths as they are prepared for analysis and when they enter the soil environment.

A Brief History of Carbon Sequestration in Phytoliths

Percentage carbon was first measured in phytoliths by Jones and Beavers (1963) who found that those isolated from a Cisne silt loam contained 0.86% carbon. They were also the first to suggest that carbon was occluded within phytoliths where it is protected from oxidation. For many years after that, papers emerged with varying estimates of the concentration of carbon in phytoliths. Table 1 gives a selection of these publications arranged in date order. It was widely recognized that different methods of preparing phytoliths will give different results, but there was little controversy over this. Usually researchers were using the same method to investigate carbon concentration in a number of species or different organs from the same plant, and they were not comparing their results with other publications that used different methods. Often measuring percentage carbon was incidental to the main focus of the investigation with workers being more interested in carbon dating or carbon isotopes. It was only after Parr and Sullivan (2005) suggested that PhytOC might be important in helping to combat climate change that the controversy really began. It now very much mattered what concentration of carbon was to be found in phytoliths.

TABLE 1

Table 1. Selected examples of %C measurements in phytoliths.

As can be seen in Table 1, in all of the early publications the preparatory techniques used by those wishing to measure PhytOC involved either wet ashing or dry ashing, and those are still the preferred methods for many workers. Essentially, wet ashing involves digestion of the plant material in strong acids and/or treatment with strong oxidizing agents such as hydrogen peroxide. In dry ashing, plant material is heated in a muffle furnace to a suitable temperature (often around 450–500°C), that will burn off the surrounding organic matter without damaging the phytoliths. The third method, microwave digestion, was first introduced by Parr et al. (2001). Parr and Sullivan (2014) compared wet ashing and microwave digestion, preferring the latter, as it kept more organic matter within certain classes of phytoliths (see below). A number of wet and dry ashing techniques were investigated by Corbineau et al. (2013), and all had some advantages and disadvantages. It would be fair to say that there is no consensus among scientists over which is the best method, and this has contributed to our problems in determining the “correct” value for PhytOC.

Parr, Sullivan and their co-workers set a firm basis for work on carbon sequestration in phytoliths. Importantly, they were able to show considerable differences between PhytOC in phytoliths from different sugarcane cultivars (Parr et al., 2009), bamboo species (Parr et al., 2010), wheat cultivars (Parr and Sullivan, 2011) and rice cultivars (Li et al., 2013b). Likewise, Zuo and Lü (2011) showed variation in PhytOC in different millet species. More recently, Sun et al. (2017) carried out an extensive survey of carbon sequestration in 51 rice cultivars, finding that there were significant differences between the amounts sequestered by different cultivars. All this work opens up the possibilities of planting certain species or cultivars which will increase carbon sequestration, and of breeding for this trait.

The work of Parr and Sullivan has been followed up and extended in China, mainly by Zhaoliang Song and his group. They have been particularly concerned to measure the potential for carbon sequestration in different environments in China: grasslands (Song et al., 2012a); wetlands (Li et al., 2013a); forests (Song et al., 2013); bamboo forests (Huang et al., 2014); and croplands (Song et al., 2014). In addition the group produced a number of reviews where they considered carbon sequestration at a global scale (e.g., Song et al., 2012b).

It seemed that the idea that phytoliths could sequester substantial amounts of carbon, and thereby help in combatting global warming, was becoming well established, but then Alexandre, Santos and their co-workers produced a series of papers reporting much lower values for PhytOC in their analyses (Santos et al., 2010; Alexandre et al., 2015, 2016; Reyerson et al., 2016). Like most of these papers Reyerson et al. (2016) concentrated on the “old carbon” hypothesis, but they did have a short paragraph looking at carbon sequestration in phytoliths. There they took the maximum PhytOC value that they found in their work (0.3%), and a phytolith stability factor of 10% (Alexandre et al., 2011), and calculated global annual carbon sequestration at 4.1 × 10⁴ tC year⁻¹. This is around 100 times lower than the 3.7 × 10⁶ tC year⁻¹ suggested by Song et al. (2014). If Reyerson et al. (2016) are correct then the amount of carbon sequestered in phytoliths would be insignificant on a global scale.

The controversy came to a peak with the publication of two papers in Earth-Science Reviews in 2016 and 2017. Firstly, Song et al. (2016) reviewed the topic from their viewpoint, and then Santos and Alexandre (2017) responded with an almost point by point rebuttal. Song et al. then wrote a reply to Santos and Alexandre (2017), but this was soon “temporarily withdrawn” by Earth-Science Reviews in early 2017, and that remains the case (in June 2019). Clearly there are serious problems here, and it is a great pity that very good scientists have ended up in such a heated debate. I will not take sides here, but try to reconcile the conflicting opinions, and to introduce some new thinking which might help sort out a rather unfortunate situation. Where is the main point of contention? Song et al. (2016) and Santos and Alexandre (2017) disagree on a number of topics, and some of these will be touched on later, but the main one is undoubtedly the true concentration of carbon in phytoliths. Song et al. (2016) routinely use a figure of 3% for PhytOC, and Santos and Alexandre (2017) think this is too high and that the figure should be 0.1–0.5%. The technique of extraction used by Song et al. (2016) is the microwave digestion technique developed by Parr et al. (2001), and Santos and Alexandre worry that this may leave organic contaminants on the surface of extracted phytoliths. The methods of preference for Alexandre, Santos and their coworkers are described in Corbineau et al. (2013), and involve dry ashing and acid digestion or alternatively acid digestion and alkali immersion. They then strongly advise checking the samples with scanning electron microscopy (SEM) and x-ray microanalysis for particles that have high C/Si ratios, and discarding those that have, thus eliminating contamination. Song et al. (2016) consider that the low PhytOC values preferred by Santos and Alexandre (2017) are caused by oxidation and over-extraction.

We appear to have reached an impasse with highly respected researchers taking up very entrenched positions. In the past this whole argument would not have happened, but it is now very important that we can determine PhytOC accurately if we are to assess its importance in carbon sequestration. The problem is that it is very difficult to obtain totally clean phytolith preparations without extracting some of the carbon from inside the structures. This may be even more difficult for cell wall phytoliths (see below). So I am uncertain that we will ever be able to give an exact figure for PhytOC, except in very rare circumstances. It is probably safer to give a range of potential concentrations for PhytOC, and to calculate carbon sequestration using a number of values. We should also remember that all the values in Table 1 are estimates of the amount of carbon that is sequestered fairly tightly within the structure of the phytolith. How do they relate to the situation in the soil? Moreover, all of the data in Table 1 are for mixtures of cell wall and lumen phytoliths. As, we shall see below the presence of two phytolith types with very different chemistries complicates matters even more.

Lumen and Cell Wall Phytoliths

Over many years of working on phytoliths I have talked with numerous scientists, seen many conference presentations, reviewed many papers, and read a lot more. I have noticed that some scientists concentrate on cell wall phytoliths and others on lumen phytoliths, and that this at least partly depends on the discipline of the scientist. Chemists and plant scientists have mostly worked on cell wall phytoliths and have a greater interest in what happens in the cell wall. It is possible that the chemists (e.g., Currie and Perry, 2007; Exley, 2015) prefer working on cell wall phytoliths because they have a matrix for deposition which makes the chemistry more interesting. The plant scientists (e.g., Coskun et al., 2018) see many important processes happening in the cell wall including transport, detoxification of metals and defense against pathogens. On the other hand, archeologists, palaeoecologists, and biogeochemists have sometimes seemed to downplay the significance of cell wall types, probably because of their perceived low stability in soils and sediments. For example, Song et al. (2017) stated that, “...C (carbon) from cell wall phytoliths may be quite labile and easily lost at an annual-decadal scale compared to C trapped in lumen phytoliths, which are likely to be much more stable at a centennial-millennial scale...” The otherwise excellent review of phytoliths in palaeoecology by Strömberg et al. (2018) paid almost no attention to cell wall phytoliths, even when considering the factors likely to increase the dissolution of phytoliths in soils and sediments.

If we are to understand this topic it is important that we have a clear idea of which phytoliths are cell wall types and which are lumen types. This can seem a simple question to answer, but experience suggests that it is not that easy, particularly just using light microscopy. Madella et al. (2005) gave us a nomenclature to classify phytoliths according to their morphology, but there was no mention of their chemistry as this was not the focus of the paper. In Table 2, I present some selected studies using transmission electron microscopy (TEM), where it is easy to determine which phytoliths are cell wall types and which are from the lumen. In TEM silica appears as electron opaque deposits, and the presence of silicon can be confirmed by x-ray microanalysis. In the context of this paper we are most interested in cell wall phytoliths, and that will bias the selection of publications in this section. The additional bias is that most of this work has been on grasses and cereals. The other methodology that is useful in some circumstances uses SEM in tandem with x-ray microanalysis (Table 3). Using SEM it is not always easy to distinguish between cell wall and lumen phytoliths and I have excluded any observations that I felt were uncertain from Table 3.

TABLE 2

Table 2. Some publications that have used transmission electron microscopy to investigate phytoliths.

TABLE 3

Table 3. Some publications that have used scanning electron microscopy and x-ray microanalysis to investigate phytoliths.

To facilitate further discussion it is helpful at this point to be able to visualize the different types of phytolith and how they develop. Figure 1 showing five potential pathways of phytolith development. In Figure 1A only the primary cell wall is silicified, whilst in Figure 1B secondary cell walls develop to almost fill the lumen and silica is then deposited on them. In the third type (Figure 1C), silica is deposited in the space between the primary cell wall and the protoplast, and eventually this fills the lumen. In Figure 1D the protoplast breaks down and silica is subsequently deposited within the lumen, entrapping some organelles and membranes. Finally, in Figure 1E silica is first deposited in part of the primary cell wall, and this later grows into the lumen. These five types are not exclusive, and other types are possible. For example, in some cases both the primary (Figure 1A) and secondary (Figure 1B) cell walls are silicified. It is also possible for silicification to begin in the primary wall as in Figure 1E, and to continue into the space between the wall and the protoplast as in Figure 1C.

FIGURE 1

Figure 1. The development of phytoliths. A schematic diagram showing five potential pathways of phytolith development. All begin with the unsilicified cell on the left. (A) The primary cell wall is silicified, but the protoplast remains intact. (B) Secondary cell walls develop to almost fill the lumen and silica is then deposited on to secondary walls. (C) Silica is deposited in the space between the primary cell wall and the protoplast, and eventually this fills the lumen. (D) The protoplast breaks down, and silica is subsequently deposited within the lumen, entrapping some organelles, and membranes. (E) Silica is first deposited in part of the primary cell wall, and this later grows into the lumen. Key: primary cell wall (yellow); cytoplasm (blue); vacuole (white); silica (black); secondary cell wall (gray).

Almost all of the work on silica deposition in roots has concerned grasses and cereals. There seem to be two main types of deposition. In the roots of Phalaris canariensis (Hodson, 1986) and wheat (Hodson and Sangster, 1989) the cell walls of the endodermis become silicified (as in Figure 1A). The sorghum root has been the most studied system, and here deposition begins in the inner tangential wall of the endodermis and the deposit then grows into the space between the wall and the protoplast (Sangster and Parry, 1976). So part of the deposit is on a carbohydrate matrix and part is not (similar to Figure 1E). In general there have been few reports of silica deposition in tissues of the root other than the endodermis.

It seems that almost all of the silica deposition in grass culms (stems) is in the outer tangential wall of the epidermis (Gartner and Paris-Pireyre, 1984; Hodson, 1986; Hodson and Sangster, 1990). Figure 2 shows a light micrograph of epidermal silicification from the wheat culm in a dry ashed preparation. The cells form a complete sheet or silica skeleton, and the long and short cells all have thin silicified walls similar to the situation in Figure 1A.

FIGURE 2

Figure 2. Epidermal silicification from the wheat culm. A light micrograph of epidermal silicification from the wheat (Triticum aestivum L. cv. Brock) culm in a dry ashed preparation (Buchanan and Hodson, unpublished).

Silicification of grass and cereal leaves is quite varied, with both lumen deposition in silica cells and elsewhere, and silica deposition in the cell walls. There has been much attention given to the silica cells (e.g., Kaufman et al., 1985; Hodson and Sangster, 1990; Laue et al., 2007). Kumar et al. (2017a) investigated the development of silica cells in sorghum leaves, and found that the deposits developed in the apoplastic space between the cell wall and the protoplast (see Figure 1C).

The inflorescence bracts of grasses and cereals have received some consideration. In the 1980s three groups all worked on the macrohairs from the lemma of P. canariensis, and Hodson et al. (1984) looked at the development of the highly thickened and silicified hairs. By maturity the hairs had only a very small lumen, and the whole wall was silicified. The long cells of the outer epidermis also considerably thickened during development, and silica was then deposited in the thickened cell wall (see Figure 1B). So in this case, what appeared to be a lumen phytolith was actually a cell wall phytolith. In the Phalaris lemma almost all phytoliths isolated from the organ were cell wall phytoliths. It is important to note that using light microscopy and SEM on this system did not indicate that these long cells were cell wall phytoliths, and that the silica was deposited on a carbohydrate matrix (Sangster et al., 1983). It is not always easy to be sure whether a phytolith has such a matrix. Long cells are very important repositories for silica in the epidermis. How many other apparently lumen types are in reality cell wall phytoliths? The Phalaris glumes, the next layer of bracts outside the lemma, are a completely different structure, with silica cells, and several different types of wall phytolith (Hodson et al., 1985).

There has been less work on silica deposition in the grass caryopsis (seed), and where present the amount is low (Hodson and Parry, 1982; Parry et al., 1984). I have included a few examples of work on silica deposition in non-grass species in Tables 2, 3: nettle, Equisetum, Cannabis, white spruce, and bracken. Recently, phytolith production in the bryophytes has also been investigated (Thummel et al., 2018), and most silica deposition seems to be in the cell walls of these plants. It seems that there is little epidermal lumen deposition outside the grasses.

This survey has, of necessity, been brief and I have left out many papers and just selected a few examples. We can conclude that the following phytoliths are definitely cell wall types: macrohairs, prickle hairs, papillae (wall). The cell walls of many epidermal cell types are often silicified, and not only in the grasses. It seems that there are some organs where cell wall silicification is the only type (e.g., grass roots and culms). Cell lumen deposition, particularly in the epidermis, is apparently more common in grasses and cereals than in the rest of the plant kingdom. Whilst it is not possible from this survey to quantify the relative importance of cell wall and lumen phytoliths it is clear that the former make up a very significant proportion of the total.

Modeling Carbon in Phytoliths

So far, we have seen that there is carbon in phytoliths, and that the amounts reported vary depending both on the sample analyzed and on the technique used to process the phytoliths. We have tried to determine precisely which phytoliths develop as silica is laid down onto a carbohydrate cell wall, and which are not. In this section we will use data that is available in the literature in an attempt to partition PhytOC between cell wall and lumen phytoliths. We will begin with cell wall phytoliths.

Perry et al. (1987) found that the macrohairs from the lemma of the grass, P. canariensis, consisted of 40% silica, 55% carbohydrate, and less than 5% protein. This is the only analysis of native cell wall phytoliths that I am aware of. It is an unusual situation where there are considerable amounts of large silicified hairs that are easy to harvest, and by maturity they consist only of cell wall phytoliths (Hodson et al., 1984). For our purposes, we need to convert the percentages for carbohydrate and protein to percentage carbon. So for 55% carbohydrate we multiply by 12/30 to obtain a value of 22% carbon. Let us then assume that the whole of the remaining 5% organic material is protein. Most proteins consist of about 53% carbon. So the proteins in the Phalaris macrohair account for about 2.65% carbon. The overall PhytOC in these hairs is therefore 24.65%. This value may or may not be typical for cell wall phytoliths, but we would expect that these phytoliths would have significantly higher carbon than lumen phytoliths. Thus, we have PhytOC for native cell wall phytoliths before any treatment to remove carbon (e.g., wet or dry ashing or microwave digestion) or degradation in the soil. This is uncommon as all other literature analyses are for phytoliths that have been treated in some way to remove external carbon. It is also important to note that all of the values quoted in Table 1 above represent those obtained from mixtures of cell wall and lumen phytoliths, and are bound to be lower than those for pure cell wall preparations.

We do not have similar data for native lumen phytoliths, but the percentage of carbon will undoubtedly be much lower than in cell wall phytoliths. The silica cell phytoliths in sorghum developed in the space between the protoplast and the cell wall (Kumar et al., 2017a). In cases like this (Figure 1C), we would expect that phytoliths would not only be low in carbohydrates, but also largely devoid of membranes, DNA and other organic compounds and have very low percentage carbon. Alexandre et al. (2015) found carbon and nitrogen spread evenly across short cell phytoliths from wheat, suggesting that there were no membrane remains, but the possibility that amino acids were present was raised (see below).

Therefore we potentially have a situation where there are two distinct classes of phytoliths that are very different in their carbon concentrations. What other evidence is there for this idea? Jones and Beavers (1963) separated phytoliths on the basis of their specific gravity, and found that those with specify gravity less than 2.10 had a carbon content of 1.6%, well above the overall sample (0.86%). In another approach, Yin et al. (2014) heated rice straw phytoliths and found that there were two pools of carbon within them. They attributed the carbon released at lower temperatures to that in the cell wall phytoliths, and that at higher temperatures was suggested to come from the lumen phytoliths. Yin et al. (2014) estimated the ratio of cell wall to lumen carbon as 12 or 13 to 1. These two different approaches both confirm that there are two types of phytolith with different carbon concentrations.

Parr and Sullivan (2014) produced the single paper that comes closest to the overall hypothesis that I am setting out here. They compared two methods of preparing phytoliths from sugarcane and sorghum, microwave digestion, and a rapid digestion using H₂SO₄/H₂O₂. The microwave digestion method was less damaging for the phytoliths and retained much more carbon. Parr and Sullivan suggested that there were two main types of phytolith, cavate, and solid. Cavate phytoliths were essentially the cell wall phytoliths of the type often seen in the epidermal long cells where the thin walls form a hollow structure. These would be similar to the situation depicted in Figures 1A, 2. Solid phytoliths were silica cells and other lumen types (Figures 1C,D). The amount of carbon found using microwave digestion was considered by Parr and Sullivan to give an accurate total value for carbon in their preparations, what they termed PhytOC_Tot (Table 4). They thought that the rapid digestion procedure removed all of the carbon from the cavate (cell wall) phytoliths, but left it in the solid (lumen) types. This was termed matrix carbon, and hence PhytOC_Mat. It is then a simple matter to deduct these matrix values from the total to give the cavate (cell wall) percentages (PhytOC_Cav). Neither value comes close to the 24.65% calculated for the Phalaris macrohair (above). This could either suggest that percentage carbon in cell walls varies considerably depending on the source, or that even the microwave digestion technique employed by Parr and Sullivan is over-extracting some carbon.

TABLE 4

Table 4. Partitioning of carbon in sugarcane and sorghum samples (Parr and Sullivan, 2014).

As an aside, I am not that keen on “cavate” and “solid” as descriptive terms, as many of the cell wall types mentioned in Tables 2, 3 above are solid. But as we have seen, even my preferred terminology of “lumen” and “cell wall” has some problems. It may be that we will need to classify phytoliths according to whether or not they are formed on a carbohydrate matrix.

At this point, I would like to introduce three concepts, PhytOC_max, PhytOC_min, and PhytOC_prep. These are in some ways related to the terms suggested by Parr and Sullivan (2014). I hope that they will prove helpful in throwing some light on the problems we have encountered with interpreting carbon sequestration in phytoliths. Firstly, PhytOC_max is the maximum amount of carbon occluded within a phytolith as it drops from a plant into the soil. This will be the amount in native phytoliths before they begin to degrade in the soil or before any attempt at preparation in a laboratory. In practice this is usually very difficult to determine. When phytoliths drop into the soil they are generally surrounded by non-silicified organic material. The aim of the preparatory techniques (dry ashing, wet ashing, and microwave digestion) is to remove all of the extraneous organic material without touching that which is bound within the phytolith structure. But it is only in very rare cases such as the Phalaris macrohairs described above (Perry et al., 1987) that we can be sure that we have accurately determined PhytOC_max. So PhytOC_max is an important, but largely theoretical, concept. Secondly, PhytOC_min is the amount of carbon remaining in a phytolith after all of the easily available carbon has been removed. Of course, this value is very likely going to differ for different types of phytoliths. We might expect that most of the carbon in cell wall phytoliths will be easier to remove, and maybe that in lumen phytoliths will be less labile. In the soil it may take a long time to reach PhytOC_min (see below for a discussion), but laboratory preparatory techniques may well approach this value very rapidly. A key question is how many of the measurements in Table 1 represent PhytOC_min and how many are closer to PhytOC_max? This leads us on to the final concept, PhytOC_prep. This is the amount of carbon left within a phytolith after it has been subjected to a suitable preparatory technique in the laboratory (the equivalent of PhytOC_Tot in Parr and Sullivan’s terminology when using microwave digestion). Of course, PhytOC_prep must lie between PhytOC_max and PhytOC_min, but exactly where is difficult to be certain, and will depend on the technique used. An important question is whether the PhytOC_prep value of 3% used by Song et al. (2016) is close to PhytOC_max? If that is the case then is the PhytOC_prep value of 0.1–0.5% used by Santos and Alexandre (2017) close to PhytOC_min? So are both Song et al. (2016) and Santos and Alexandre (2017) “correct,” but the PhytOC values they give just represent what is present at different times in phytolith degradation and dissolution? We will have more to say on this point below.

Next we need to investigate mixtures of different types of phytoliths. As, we saw above there are some cases where we are fairly sure that nearly all of the phytoliths in an organ are cell wall types (e.g., the wheat root, and the Phalaris lemma), but in many cases, particularly in the grasses, there will be a mixture of both cell wall and lumen types. The evidence presented here and in my previous publications (Hodson, 2016, 2018) strongly suggests that the two types have very different chemistries, and that cell wall types have much higher carbon concentrations. So, when we have two phytolith types with different PhytOC, how do we calculate the overall PhytOC for the material? To do this, we need to have some estimates of PhytOC for both lumen and cell wall types, and some idea of the relative amounts of the two types of phytolith in a particular sample. Once, we have those estimates we can use the following equation:

$$(\text{a}\times \text{y}/100)+(\text{b}\times \text{z}/100)=\mathrm{Total\; Percentage\; PhytOC}\left(1\right)$$

Where:

a = Percentage PhytOC in lumen phytoliths;

b = Percentage PhytOC in cell wall phytoliths;

y = The percentage of lumen phytoliths in a sample (out of 100);

z = The percentage of cell wall phytoliths in a sample (out of 100) (note this formula is constrained by the fact that y + z must equal 100).

We can then investigate a variety of potential scenarios:

(1) Let us assume that PhytOC for the cell wall phytoliths is 24.65%, as in the Phalaris macrohairs (above), and that lumen PhytOC is 0.33%. The latter is the mean of the two values given by Parr and Sullivan (2014) for lumen (solid) phytoliths, and is not very different to the 0.3% used by Reyerson et al. (2016) in their calculations on global carbon sequestration.

(2) Let us use the estimates provided by Parr and Sullivan (2014) for sugarcane PhytOC: cell wall, 10.12%; lumen, 0.15% (Table 4).

(3) Similarly, the Parr and Sullivan (2014) estimates for sorghum PhytOC: cell wall, 3.37%; lumen 0.51%.

Figure 3 shows the effects of varying the ratio of cell wall to lumen phytoliths, moving from a situation where none of the phytoliths are cell wall types to where there are 100% in a sample. As would be expected, for all three scenarios, a higher percentage of cell wall types leads to a higher total PhytOC. In general Scenario 1 gives higher total PhytOC values under almost all conditions. It is interesting to calculate the percentage of cell wall phytoliths that would be required to reach the 3% total PhytOC figure that is given by Song et al. (2016) and that is used in many of the other papers from their group. For Scenario 1 only 11% of cell wall types would be needed, for Scenario 2 (sugarcane) the figure is 29%, and for Scenario 3 (sorghum) it is 88%. Clearly there is very big variation in these figures, but at least in some scenarios a relatively small percentage of cell wall phytoliths would be needed to bring us close to the 3% figure that Song et al. (2016) preferred.

FIGURE 3

Figure 3. The effects of mixing different amounts of cell wall and lumen phytoliths on total PhytOC. Potential scenarios: (1) PhytOC for the cell wall phytoliths is 24.65% and PhytOC for lumen phytoliths is 0.33%. (2) PhytOC for the cell wall phytoliths is 10.12% and PhytOC for lumen phytoliths is 0.15%. (3) PhytOC for the cell wall phytoliths is 3.37% and PhytOC for lumen phytoliths is 0.51%.

As far as I am aware nobody has attempted to quantify the relative volumes of cell wall and lumen phytoliths in organs like the grass leaf, and this is an important topic for future research. Another key subject arising from this work concerns differences in carbon allocation between species and cultivars. As we saw above, Parr, Sullivan and their team found major differences between PhytOC in phytoliths from different bamboo species, and sugarcane, wheat, and rice cultivars. It has been suggested that it might be possible to breed plants for high PhytOC. But at the cellular level what are we breeding for? Is it simply a change in the ratio of cell wall to lumen phytoliths? Or is it more complex than that?

Some Thoughts on Carbon and Nitrogen in Phytoliths

There have been few measurements of nitrogen in phytoliths to date. The presence of nitrogen would indicate that proteins, amino acids, and possibly nucleic acids had been incorporated into the phytoliths. Most proteins contain about 53% carbon and about 16.3% nitrogen so their C/N ratio will be about 3.25. Values higher than that would suggest that carbohydrates and/or lipids were a significant part of the carbon present in the phytoliths. Table 5 shows the data that I have been able to locate concerning nitrogen concentrations in phytoliths.

TABLE 5

Table 5. Phytolith carbon and nitrogen analyses.

Jones and Beavers (1963) were the first to measure nitrogen in phytoliths at 0.01%, which would give a C/N ratio of 86. The accuracy of this C/N ratio is probably somewhat questionable given the very low nitrogen concentration, and the age of the work. I was able to calculate the percentage nitrogen in the Phalaris macrohairs studied by Perry et al. (1987). They estimated that percentage protein in the hairs was less than 5% and so the maximum percentage nitrogen will be 0.82% at PhytOC_max in native hairs before treatment. Using the previously calculated value for percentage carbon of 24.65% we can determine that the C/N ratio of Phalaris macrohairs is a minimum of 30. Hodson et al. (2008) measured nitrogen in phytoliths extracted from various wheat organs using dry ashing followed by boiling in hydrogen peroxide. They found low, but detectable, amounts of 0.01–0.06% nitrogen. The calculated C/N ratios varied from 7 to 43, depending on the organ, with the bulk sample containing all organs giving a value of 41. Fragmented glycoproteins were found in wheat leaf phytoliths by Elbaum et al. (2009), confirming the presence of nitrogenous compounds, although they did not quantify the amounts. The leaf short cell phytoliths of Triticum durum were analyzed using nanoSIMS by Alexandre et al. (2015). They were not able to quantify carbon and nitrogen concentrations, but their C/N ratio was 3.7. In the following year, Alexandre et al. (2016) wet ashed the leaves of Festuca arundinacea and found that the phytoliths had a C/N ratio of 5.1.

How do we interpret the above data? Firstly, it is striking that the values for C/N ratio in Table 5 fall into two groups with the rachis of wheat and the analyses conducted by Alexandre et al. (2015, 2016) giving markedly lower values than the rest. The value for native Phalaris macrohairs calculated from Perry et al. (1987) gives an approximate baseline for cell wall phytoliths with a minimum C/N ratio of 30. It seems that the C/N signature for cell wall phytoliths dominates the wheat samples analyzed by Hodson et al. (2008) even after they have undergone dry ashing and boiling in hydrogen peroxide. Alexandre et al. (2015) were quite correct to point out that their nanoSIMS analysis for leaf short cells strongly suggests the presence of amino acids with a C/N ratio of 3.7 in these lumen phytoliths. This forms a baseline for lumen phytoliths. When Alexandre et al. (2016) wet ashed F. arundinacea leaves, the phytoliths within them had a slightly higher C/N ratio of 5.1, again suggesting dominance of amino acids and proteins. It seems very likely that the extraction procedure used by Alexandre et al. (2016) was stronger than that used by Hodson et al. (2008), and that they removed most of the carbon from within the cell wall phytoliths, leaving that in the lumen phytoliths largely intact. This thinking is along similar lines to that of Parr and Sullivan (2014), where cell wall (cavate) phytoliths were considered to be more susceptible to extraction than lumen (solid) phytoliths. The wheat rachis sample had very low carbon and nitrogen in its phytoliths, and I suspect that this relatively lightly silicified organ was also over-extracted. More work is needed employing C/N ratios for phytolith analyses to confirm these ideas, but this ratio certainly seems to have potential for assessing the relative contributions of carbohydrates and amino acids within a processed sample.

The Loss of Carbon From Phytoliths in the Soil and Sediments

The evidence I have presented so far in this paper very strongly suggests that lumen phytoliths generally have low PhytOC. Even Parr and Sullivan (2014), the originators of the carbon sequestration in phytoliths idea, are proposing values as low as 0.15–0.51% (Table 4). As, we saw above, Reyerson et al. (2016) calculated global carbon sequestration using a PhytOC of 0.3%, assuming that this applied to all phytoliths, and concluded that sequestration would be insignificant. So if lumen phytoliths are not that important for carbon sequestration the whole hypothesis hangs on the cell wall phytoliths. However, the general assumption is that cell wall phytoliths are less likely to remain in soil as they are more easily broken down (Song et al., 2017). But is this really the case?

Strömberg et al. (2018) have produced a very detailed assessment of what happens to phytoliths when they enter the soil, and we will not go back over all of this material, but mostly concentrate on any differences between cell wall and lumen phytoliths. It is clear that, in many soil environments, a considerable amount of siliceous plant material, including phytoliths, breaks down fairly quickly. Indeed, phytoliths are often an important source of dissolved Si in soils as they are much more soluble than quartz, aluminosilicates, and other soil minerals. Working on a temperate coniferous forest, Gérard et al. (2008) showed that 60% of the biogeochemical cycle was controlled by biological processes, namely Si uptake by plants and dissolution of phytoliths. There is a large labile pool of phytogenic silica in soils (Strömberg et al., 2018), with values for this pool ranging from 69% in short grass prairie to 92% in tropical forest.

Puppe et al. (2017) conducted a detailed analysis of the contribution of biogenic silica to the soil soluble silicon pool at Chicken Creek in Brandenburg, Germany. They considered diatoms and sponge spicules in addition to phytoliths, but it was the latter that were by far the most important in contributing to soluble silicon concentrations in the soil. However, they discovered that small, delicate, phytolith fragments which were not usually quantified using standard extraction processes made up 84% of the phytogenic material and those larger than 5 μm represented only 16%. The authors stressed the importance of this large pool of small delicate material in contributing to soluble silicon in the soil. The micrographs of the fragile phytoliths they showed (their Figure 7) were not that dissimilar to my Figure 2 with thin cell wall silicification. Clearly these structures would be highly susceptible to dissolution. Presumably the larger phytoliths that represented 16% of the phytogenic material would remain in the soil for much longer periods.

At the global scale, the phytolith stability factor was one of the disagreements between Song et al. (2016) and Santos and Alexandre (2017). The former suggested a stability factor of 0.8 to 1.0 as phytoliths in most systems are stable for 500 to 3000 years. However, Santos and Alexandre (2017) suggested a stability factor of 20%, which combined with their much lower value of PhytOC (0.3%), led them to suggest that carbon sequestration in phytoliths on a global scale was insignificant. As we saw above, it seems very likely that the value of 0.3% PhytOC used by Santos and Alexandre is an underestimate due to over-extraction, and that particularly applies to cell wall phytoliths. It is difficult to speculate on the influence of cell wall phytoliths on the stability factor as we lack even basic data.

Next we will investigate the dissolution of lumen and cell wall phytoliths. I recently reviewed this topic (Hodson, 2018), and a number of factors seem to be important. Of the soil chemical factors, high pH was the most significant, causing increased phytolith dissolution. It is possible that aluminum in phytoliths may decrease their dissolution, but their carbon content hardly seems to have been considered. Cabanes and Shahack-Gross (2015) carried out the most detailed work so far on this topic but, with the exception of the double peaked glume phytoliths from rice husks, most of their work concentrated on lumen types. The key factor in increasing phytolith solubility was geometric surface to bulk ratio. There was no indication that cell wall phytoliths were either more or less soluble.

We should now consider what is known about cell walls that have undergone silicification. The small number of measurements so far available for carbon in cell wall phytoliths shows considerable variability (see above: Perry et al., 1987; Parr and Sullivan, 2014). If the percentage carbon is high then percentage silicon must be low and vice versa. We would not necessarily expect all cells walls to be silicified to the same extent, but this will mean that they will vary in their chemical properties, and potentially in how susceptible they are to breakdown processes in the soil. I previously discussed evidence that suggests that after the organic matter is removed from cell wall phytoliths the remaining silica has a porous structure (Hodson, 2016). Since that publication, Sola-Rabada et al. (2018) have published the first estimate of the size of the pores that I am aware of. In phytoliths isolated from Equisetum myriochaetum using wet ashing the silica had a surface area of ∼400 m² ⋅ g⁻¹ and a pore size of ∼5 nm. Presumably, in the native state these pores will have been filled by carbohydrates and other organic compounds. Almost certainly pore size will vary, and we might expect more lightly silicified material to have larger pores. But we should remember that these cell wall phytoliths are only porous after most of the organic matter has been removed with drastic treatment. Will cell wall phytoliths necessarily be more susceptible to breakdown in the soil than lumen types just because they have higher organic matter within them? Does being encrusted by silica slow down the microbial degradation of organic matter in phytoliths? Conversely, does being so intimately associated with organic matter impede the dissolution of silica from phytoliths? We do not know the answers to these questions yet.

There is not very much known about how silica and organic matter are associated in the soil. However, the work of Watteau and Villemin (2001) on the breakdown of leaves and roots soils of a beech forest is important in this respect. Using TEM and electron energy loss spectroscopy (EELS) they found silica was deposited in beech leaves in the walls of the epidermal and parenchymatous cells, in the middle lamellae, against the walls in the cells, or in cell intersections. The authors stressed the close relationships between biogenic silica and cellulose, hemicellulose, and pectic substances in these samples. Deposition was in similar locations in the cell walls of beech roots, but also in the root cortical cells closely associated with polyphenolic substances. In the soil the leaf and root tissues were broken down primarily by fungi, but bacteria were also present. The fungi attacked the carbohydrates in the cell walls, leaving the silica largely intact, particularly that in the cell intersections. More recently, Turpault et al. (2018) also investigated silicon cycling in beech forests. Much of the silicon was associated with cell walls in the beech tissues. Turpault et al found that fine beech roots were particularly important in cycling as they had a high Si content and were rapidly broken down and recycled. Very little Si was lost from the system through deposition in perennial tissues or leaching from the soil, and it was an almost closed system. It is clear from both Watteau and Villemin (2001) and Turpault et al. (2018) that cell wall Si deposition is the most important in beech, and in the soils beneath the forests. The papers also give us some insights into breakdown of cell wall phytoliths in soils and how rapid this can be. The beech cell walls investigated appear to be fairly thin and relatively lightly silicified (similar to Figure 1A), and it would be unwise to extrapolate from this situation to others where heavier silicification has occurred.

As I was writing this paper, the Intergovernmental Panel on Climate Change (IPCC) brought out their 2018 report on the feasibility of keeping the global temperature rise under 1.5°C above the pre-industrial temperature. The report has a section (4.3.7.3) which considers increasing carbon sequestration in soils as one of the means of tackling the problem (de Coninck et al., 2018). At a local scale the benefits of increasing carbon sequestration in soils are clear, but there is much uncertainty about how much carbon can be sequestered at a global scale and what the costs might be. The section does consider work on the use of biochar to increase sequestration but, rather like work on phytoliths, there is considerable debate about its potential. Not surprisingly, the idea that phytoliths might be involved in carbon sequestration in soils has not yet impinged on the IPCC. We will need much more work and much greater certainty before that might happen.

Before we leave this topic, I have one more question to raise. How long do we need to sequester carbon? There seems to be a general assumption in the phytolith literature that we need to sequester carbon for hundreds or thousands of years, and that sequestration for shorter periods is not worthwhile. Parr and Sullivan (2005) found phytoliths from 8710 BP at Byron Bay in Australia still contained PhytOC, and so sequestration is possible for very long periods of time. However, I would argue that the problems that we are having with climate change are so severe that we need to maximize short term sequestration, and that even locking away carbon in phytoliths for 50 or 100 years might make a valuable contribution. In that time we might hope that the world will make the switch to renewable technologies, and that we might have developed other methods for sequestering carbon. The IPCC have made it very clear how urgent the problem of climate change is, and the short time scales involved to reduce what could be very serious impacts. We need to keep this in mind as we investigate carbon sequestration in phytoliths.

Do Cell Wall Phytoliths Remain in Archeological and Palaeoecological Samples?

In the previous section, we investigated what is known about the chemistry of phytolith breakdown and dissolution in the soil and sediments. It is highly unclear whether cell wall phytoliths are degraded faster than lumen phytoliths as there is little data available. Since this is the case, we will now turn to the archeological and palaeoecological literature to investigate whether cell wall phytoliths persist in soils and sediments.

As we have seen earlier it is not always easy to determine whether a phytolith has a carbohydrate matrix, so we will confine this survey mostly to macrohairs, prickle hairs and papillae (Table 6). The double-peaked rice husk phytoliths are also cell wall phytoliths occurring on the outer surface of the rice husk, and they are heavily silicified (Park et al., 2003). An additional category we will add are multi-celled phytoliths, also known as silica skeletons (Rosen and Weiner, 1994). These are groups of phytoliths frequently, but not only (see Figure 2), originating from the husks of cereals. They often contain papillae within their structures, and will inevitably enclose cell walls between the different cells. Included within the silica skeletons are the cut phytoliths which appear in archeological contexts, and are diagnostic for cutting and threshing activities (Cummings, 2007).

TABLE 6

Table 6. Cell wall phytoliths in archeological and palaeoecological samples.

Table 6 represents the results of a partial survey of the literature, and there are many other papers that could have been cited. However, it is clear that cell wall phytoliths can be found in samples that are hundreds or thousands of years old. In two cases (Prasad et al., 2005; Wu et al., 2018) they were found associated with dinosaur remains from the Cretaceous. Here, we would expect that the phytoliths discovered will be fossilized and have lost their original organic matter, but it does indicate that they persisted long enough to be preserved in this way. Cell wall types have been found in many different contexts and environments, from extremely arid to temperate, and in many different countries. It would not be wise to attempt any sort of quantification, particularly as we are uncertain how many long cell phytoliths have a carbohydrate matrix (see Figure 1B and discussion above). I have included both archeological and palaeoecological examples in Table 6. It could be argued that archeological contexts do not always replicate conditions from the natural environment. However, it is now recognized that agriculture is having a major impact on the global silicon cycle (Struyf et al., 2010), and so, to some extent, the work on past agricultural activity is an analog for what is happening today. Moreover, much of the work on increasing carbon sequestration in phytoliths in the future concerns agricultural crops (Parr and Sullivan, 2011).

In conclusion, the small survey shown in Table 6 has strongly indicated that cell wall phytoliths can persist in soils and sediments for considerable periods of time. It is conceivable that these cell wall phytoliths may have lost much of their organic matter over time, but that their basic structure remains intact. It is, however, more likely that they still contain substantial amounts of carbon hidden deep within the phytolith structure. So we are faced with the possibility that some carbon may be sequestered in cell wall phytoliths for hundreds or thousands of years. But as we argued above, the more important issue is how much carbon is sequestered for short periods of time, maybe 100 years.

A Hypothesis

Having gathered together data and observations from many different sources I am now able to put forward a hypothesis which attempts to explain the overall picture. First, let us reflect on what happens when phytoliths are prepared for analysis by wet ashing, dry ashing or microwave digestion:

(1) The non-silicified material is rapidly removed to expose the phytoliths. The phytoliths are then at PhytOC_max.

(2) The more porous cell wall phytoliths will be more vulnerable to carbon loss than the lumen phytoliths.

(3) If the extraction procedure is not too severe then carbon will remain in both cell wall and lumen phytoliths. The PhytOC_prep value arrived at will depend on the severity of the extraction procedure.

(4) If the process is more severe then all the cell wall phytolith carbon will be lost, but that in the lumen phytoliths will be much less affected. Here, we reach PhytOC_min.

(5) Only if extreme procedures are used will all the carbon be lost from all phytoliths. For example, Yin et al. (2014) showed that at very high temperatures (above 900°C) most carbon is removed from rice and millet phytoliths.

Now let us consider the situation in the soil:

(1) When plant material falls into the soil or becomes incorporated into it, cell wall and lumen phytoliths are all surrounded by non-silicified material.

(2) Depending on the soil conditions the non-silicified plant matter rots fairly quickly to expose the phytoliths within it. The phytoliths are then at PhytOC_max.

(3) The lumen phytoliths contain a small amount of carbon, but are resistant to breakdown in the soil.

(4) The cell wall phytoliths contain a much larger amount of carbon, but are more easily broken down in the soil.

(5) Within a short period of time (a few decades) much of the smaller, lightly silicified cell wall and intercellular silica deposition breaks down. The silica dissolves and the organic material contained within it undergoes decomposition and is released back to the atmosphere as carbon dioxide.

(6) The remaining cell wall and lumen phytoliths then dissolve and break down more slowly over centuries or millennia. It may be a very long time before they reach PhytOC_min.

(7) Depending on the plant species and organs that originally contributed the phytoliths either the lumen or cell wall deposits are the more important in sequestering carbon in the soil. This part of the hypothesis requires further exploration, and this is carried out below.

From the work of Watteau and Villemin (2001) and Turpault et al. (2018) it is evident that cell wall phytoliths are the most important in the soils of beech forests. I am not aware of similar work for the soils of coniferous forests. However, my previous work on conifer needles has strongly indicated that cell wall deposition is important in this group. For example, Hodson and Sangster (1998) found that silica deposition was almost entirely confined to the hypodermal and endodermal walls of white spruce needles. Presumably this would be reflected in the phytoliths to be found in the soils of conifer forests. In grasslands it is probable that lumen phytoliths (particularly short cells) will dominate in most phytolith assemblages isolated from soils. In these cases we may need to balance a very large number of lumen phytoliths that contain small amounts of carbon against a smaller number of cell wall phytoliths that contain much more carbon. It may be that a modified form of Equation 1 could be used in these circumstances to determine the overall PhytOC percentage. Very recently, Zhang et al. (2019) showed the importance of bamboo litter layers in carbon sequestration, and demonstrated the considerable potential that exists to increase carbon sequestration in the future. But what types of phytoliths might we expect to dominate the litter layers? Firstly, it is clear that bamboo leaves contain much higher silicon concentrations than the other organs (Collin et al., 2012), and these will undoubtedly be the major contributor to phytoliths in the litter. Lux et al. (2003) investigated silicification of bamboo (Phyllostachys heterocycla Mitf.) leaves and found the highest Si concentrations were in the epidermal cell walls and short cells. This suggests that bamboo litter should contain both cell wall and lumen phytoliths. Which will be dominant in the litter is uncertain. We have seen that bamboo species differ in the amount of PhytOC within their phytoliths (Parr et al., 2010), and we might also expect that the litter will vary in the relative amounts of cell wall and lumen phytoliths, depending on the species involved.

I am not clear whether lumen phytoliths or cell wall phytoliths will be the more significant in sequestering carbon at a global scale. At the moment we have not got enough data even to make an informed guess on the relative importance of the two phytolith types in carbon sequestration at this scale.

Priorities for Future Research

A number of important research topics have arisen from the present study:

(1) We have seen that there is some uncertainty about which phytoliths are deposited on a carbohydrate matrix. This is particularly the case for long cells. Hodson et al. (1984) showed that silica was deposited onto thickened secondary cell walls in the long cells of the outer epidermis of the lemma of P. canariensis (similar to Figure 1B). I am not aware of any other examples of this phenomenon, but surely it cannot be the only case? Long cells are important sites of silica deposition, and if it were discovered that the lumen of many had a carbohydrate matrix they could be very significant repositories for carbon sequestration. The work would require plant scientists (probably) to use TEM and x-ray microanalysis following a developmental sequence as the cells silicified.

(2) What is the ratio of cell wall to lumen phytoliths in organs where they are both present? If we knew this we would have data that could be used in Equation 1. We would then be able to assess the relative importance of cell wall and lumen carbon sequestration. This work probably requires microscopy and image analysis.

(3) We know from the work of Parr, Sullivan and others that there are differences between cultivars in PhytOC. But what is the difference at the cellular level? There have also been suggestions that it might be possible to breed for high carbon sequestration in phytoliths. Are we breeding for a change in the ratio of cell wall and lumen phytoliths? Again this work will require microscopists and image analysis.

(4) It appears that the C/N ratio of phytoliths might have some promise in indicating whether preparations are dominated by amino acids or carbohydrates and whether samples are over-extracted, but this work needs to be expanded. For instance, it would be of great interest to repeat the work of Parr and Sullivan (2014) using both drastic wet ashing and gentler microwave digestion preparative procedures, and then analyze for both C and N. If my thinking above is correct I would predict that the wet ashing preparation will have a lower C/N ratio than that obtained through microwave digestion.

(5) We need to determine whether the breakdown and dissolution of cell wall phytoliths is faster than that of lumen phytoliths in experimental situations. Here, we could repeat the work of Cabanes and Shahack-Gross (2015) on phytolith dissolution, but specifically comparing cell wall and lumen phytoliths.

(6) In the soil, we have a very incomplete picture of the processes involved in phytolith dissolution, and even more so for cell wall phytoliths. More work of the type described by Watteau and Villemin (2001) on beech forest soils is needed.

(7) Parr and Sullivan (2005) found carbon in phytoliths from 8710 BP. We have seen that cell wall phytoliths can remain in archeological and palaeoecological samples for hundreds or thousands of years, but does carbon remain within them? If so it would suggest the potential for high carbon sequestration, but if not then cell wall phytoliths must be strong even once carbohydrates have been removed.

My Conclusion and Perspective

I said at the beginning of this paper that I would not take sides in what has become an acrimonious debate over carbon sequestration in phytoliths. However, having carried out a detailed analysis and weighed up all the evidence I conclude that the hypothesis that carbon sequestration in phytoliths is important on a global scale is probably correct, or at least cannot yet be discarded. I think it is likely that all workers in this area (and I include myself) have over-extracted phytoliths, and that we have not given an accurate representation of PhytOC_max. It is probable that Alexandre, Santos and their co-workers have over-extracted to the point where their preparations are approaching PhytOC_min. I am very clear that we have all not taken enough account of heterogeneity in phytolith chemistry. It seems very likely that cell wall phytoliths are important in carbon sequestration, and it may even prove to be the case that they are more significant than the lumen types. In this paper I have considered lumen and cell wall phytoliths, but it is quite possible that this is an oversimplification and that there are more than two types or some gradation between the two (e.g., the situation in Figure 1E). There is no doubt that what I have presented here makes the whole topic of carbon sequestration in phytoliths even more complex than it was, but if we are to move this field forward then these complexities need to be accounted for.

I have worked on phytoliths for nearly 40 years. Much of my work has been what some people call “blue skies” research. That is it had no obvious immediate practical application. So, I have been quite surprised that some of my publications on microanalysis and phytolith development from the 1980s now have a new relevance in 2019 when we consider carbon sequestration and PhytOC. I suspect that quite a few of the authors cited in this paper will be equally surprised. I do worry that financial pressures mean that we are losing the possibility to research topics just because they are interesting.

Many scientists from very diverse disciplines have contributed to the picture I have painted in this paper. However, if we look specifically at the question of carbon sequestration in phytoliths a few people stand out. Foremost among these must be Jeffrey Parr and Leigh Sullivan who first had the idea that phytoliths might sequester substantial amounts of carbon. All of the data was already there for everyone to see, but they had the idea, and the sudden spark of brilliance that really created a whole new field of phytolith research. They then carried out a considerable amount of work to test their hypothesis, and particularly to look at variation in carbon sequestration in phytoliths from related species and cultivars. If Parr and Sullivan were the originators of the idea, then Zhaoliang Song and his team in China were those who tested it out in a whole string of investigations. We should also be grateful to Ann Alexandre, Guaciara Santos and their co-workers who “shook the tree” and made us all wonder if sequestration of carbon in phytoliths was an important phenomenon. I disagree with their overall conclusion on the importance of carbon sequestration in phytoliths, but they are very good scientists and have done some excellent work in this area. It was through their work that I hit on the concept of PhytOC_min, which I have described above. They also provided some useful data on nitrogen in phytoliths which was crucial in my thinking about C/N ratios. Finally, I must mention Carole Perry, whose work on the chemistry of phytoliths has been seminal. I used some of her early research to develop the idea of PhytOC_max, and in many ways her analysis of the Phalaris macrohair (Perry et al., 1987) was the key to unlocking this puzzle. I am sure that Carole would never have guessed back in the 1980s that her work would be used in this way. For me this is a fascinating story that has developed over more than 30 years. It is notable that much of the research I have based my ideas on was originally “blue skies,” but now it makes a significant contribution to a very important topic.

As I write in 2019, the evidence for the effects of human-induced climate change is all too obvious from around the world. The IPCC report (2018) that I mentioned above laid out what we need to do to avoid a very perilous future. For the last 15 years I have spent much time speaking and writing about climate change for general, non-scientific audiences (Hodson and Hodson, 2011, 2013, 2015). Every new talk I prepare or article I write about climate change makes me aware of just how serious and urgent this issue is. Now I am approaching my 40th anniversary of working on phytoliths, and we can see that they might have a potential role in carbon sequestration in soils. I am not convinced that phytoliths will be a “silver bullet” for climate change, but the work described above suggests that they may have a role to play. We now really need a concerted and determined effort from the whole phytolith community to test out some of the ideas laid out above. There are key topics for scientists from many different disciplines to work on, from those investigating phytolith chemistry and formation at a molecular level right up to those studying biogeochemical cycles. It is extremely important that we maintain very good communications between all these scientists, and not end up in disciplinary boxes. There is a lot to recommend the phytolith superdiscipline idea of Katz (2018), where boundaries between disciplines are dissolved.

There has been considerable tension within the phytolith community over carbon sequestration in the last few years, and academic disagreements have turned to friction and friction to heat. I sincerely hope that all of the scientists working on carbon sequestration in phytoliths will one day be reconciled (and reconciliation is even more needed where dating of phytoliths is concerned). This issue is too important for personal rivalries to get in the way. I would appeal for all involved to work together toward a common goal. That goal is working out how important PhytOC is, and if it is important then finding ways of using the knowledge gained as quickly as possible. Put aside previous arguments and get on with the job. I will gladly work with anyone who wants advice or help, and I will not be upset if some of the thinking above is incorrect. I have put forward a hypothesis which seems to explain the available data, but it is a hypothesis and it needs testing. If, in 10 years’ time, someone writes, “Hodson got it totally wrong, but he gave me some ideas, and now we have it right,” then I will be very happy.

Author Contributions

The author confirms being the sole contributor of this work and has approved it for publication.

Conflict of Interest Statement

The author declares that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.

Acknowledgments

I would like to dedicate this paper to the memory of my friend and colleague, Allan Sangster who died on September 6, 2018, aged 91. I published more papers with Allan than with anyone else, and it is fair to say that without him the present paper would never have happened. I am particularly grateful to my wife, Margot, for allowing me to bounce ideas off her for this paper. Even more grateful as sometimes our conversations were in the early hours of the morning! With all my love Martin.

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