HESS Opinions: Unsaturated infiltration – the need for a reconsideration of historical misconceptions
- 1Department of Geography, University of Bern, Bern, Switzerland
- deceased, 6 December 2020
Correspondence: Keith Beven (firstname.lastname@example.org)
Briggs (1897) deduced capillary flow from deviation of the equilibrium between capillarity and gravity. Richards (1931) raised capillary flow to an unproven soil hydrological dogma. Attempts to correct the dogma led to concepts of non-equilibrium flow, macropore flow, and preferential flow during infiltration. Viscous film flow is proposed as an alternative approach to capillarity-driven flow during unsaturated infiltration.
Editorial note to close the review process of the article “Unsaturated infiltration: from unproven capillary flow to viscous flow" by Peter F. Germann.
Peter Germann submitted the first version of this opinion paper on 26 October 2020 to HESS. Together with two other scientists, John R. Nimmo kindly accepted to review this work in early November. Shortly after, I was shocked and deeply saddened to learn that Peter Germann had passed away rather suddenly on 6 December 2020 in Bern. While I succeeded in informing two reviewers, I did not manage to reach John Nimmo because he had retired in the meantime, and his official email account was switched off. As a result, John Nimmo reviewed the manuscript without knowing about Peter Germann’s death and submitted his comment on 19 January 2021.
I am very grateful to Keith Beven, who kindly offered to address John Nimmo’s insightful comments in the revised and consequently accepted manuscript and to add a preface in memoriam of Peter Germann’s life and scientific legacy.
Erwin Zehe, Executive Editor of HESS
The paper that follows was submitted to HESS by Peter Germann in September 2020. Unfortunately, before the processing of the paper could be completed, Peter passed away rather suddenly on 6 December 2020 in Bern, Switzerland, after two major strokes. Peter was well known to many soil hydrologists for his work on preferential flows: a career of research work that was summarised in his 2014 book on the subject published by the University of Bern (Germann, 2014).
Peter and I had been good friends since we first met and started doing fieldwork together at the Institute of Hydrology at Wallingford in 1979, where he spent a year as a postdoc, and we found we had a common interest in preferential flows. Beven and Germann (2013) include some information and a photograph of the tracing experiment we did at Grendon Underwood in 1979. This was instructive in that it was done at the end of the winter on well-wetted clay soil when all the cracks in the clay should have been closed. In fact, it took the Rhodamine dye we added at the surface some 45 s to reach a mole drain at a depth of 60 cm, and destructive sampling after the trace showed that the cracks were still transmitting water (and that the grass roots were mostly on the surface of the peds).
Peter was born in St. Gallen, Switzerland, in 1944. He grew up in Bischofszell and later completed his schooling in St. Gallen. In 1963–1969 he studied to obtain a degree in forestry at ETH Zurich, and then he stayed with Professor Felix E. Richard to carry out research towards a PhD at the Eidgenössische Forschungsanstalt für Wald, Schnee und Landschaft (WSL) from 1969 to 1976. He continued his work in the Laboratories of Hydraulics, Glaciology and Hydrology (VAW) during the period 1976–1980. His PhD work was a study of the water relations on a forested slope in the Rietholzbach catchment based on maintaining a network of 35 nests of tensiometers at 10 different depths down to 3 m, set out on a triangular grid amongst the trees. At this time these were still manual tensiometers coupled to mercury manometers that were read every 2–3 d for 3 years. One of the features that this remarkable data set revealed was that during infiltration wetting could occur at depth in some cases, apparently bypassing the tensiometers above. Another was the large heterogeneity in responses between sites and between wetting events.
Peter returned to Switzerland from Wallingford, and then in 1980 he took up a post as assistant professor in the Department of Environmental Sciences at the University of Virginia (UVA) in Charlottesville, where we overlapped again for 2 years. Peter stayed at UVA until 1986. He then took a position as an associate professor in the Department of Soils and Crops at Rutgers University. In 1989 he was offered a professorship at the Institute of Geography, University of Bern, back in Switzerland, where he stayed until he retired in 2009. He held an emeritus position at Bern until 2015.
For the major part of his research career, Peter was a strong advocate for a reconsideration of the physics of water flow through soils and, in particular, for the limitations of the Darcy–Buckingham–Richards flow theory that is based on an assumption of the equilibration of capillary potentials in some (not clearly defined) “representative elementary volume” of soil pores. The paper that follows is a continuation of that theme.
Our common interest resulted in the highly cited review paper in Water Resources Research on macropores and water flow in soils (Beven and Germann, 1982), as well as a sequence of three papers in Journal of Soil Science (Germann and Beven, 1981a, b; Beven and Germann, 1981) including a modelling approach based on kinematic wave theory that received very critical reviews. Some soil physicists at that time appeared to believe that the physics of soil physics had been solved (and that still seems to be a common belief and still apparent in much teaching of soil hydrology). In 1985, we both attended an international workshop on water and solute movement in heavy clay soils, held in Wageningen (Beven and Germann, 1985), where we presented a paper on flow in distributions of macropores based on the kinematic wave approach. In the bar one evening we had a long discussion over a beer with John Philip, who argued that it would not be possible that film flow in a macropore, which would have a curved meniscus and therefore a potential at less than atmospheric pressure, could result in an outflow at the base of an undisturbed column since a positive pressure would be required. I have never been able to decide whether John was really serious in his argument, or whether he was just teasing these two earnest young men committed to the importance of preferential flows.
Peter later developed the kinematic wave approach into a theory of viscosity
(rather than capillarity)-dominated film flows subject to Stokes' law during
infiltration. This is still somewhat contentious (see the comment on the
paper by John Nimmo at https://hess.copernicus.org/preprints/hess-2020-499/), and Peter rather
glossed over issues such as the change of parameters that might be expected
as smaller pores and pore necks involved in the film flow became filled and
that require some effective parameter values. As he demonstrates in his
book, he felt that the approach was supported by both the field and
laboratory evidence. Peter was a careful experimentalist and made use of a
variety of time domain reflectometry and sonic and tracer experiments to study
preferential flows. His thoughtful and good-humoured approach to
collaborations, discussions, and presentations will be missed by many in soil
science. A more complete biography and account of Peter's contributions can
be found at http://www.history-of-hydrology.net/mediawiki/index.php?title=Germann,_Peter (last access: 1 March 2021).
Keith Beven, Lancaster University
Beven, K. J. and Germann, P. F.: Water flow in soil macropores, II. A
combined flow model, J. Soil Sci., 32, 15–29, 1981.
Beven, K. J. and Germann, P.: Macropores and water flow in soils, Water Resour. Res., 18,
Beven, K. J. and Germann, P. F.: A distribution function model of
channelling flow in soils based on kinematic wave theory, Proceedings of the International Symposium on Water and Solute Movement in Heavy Clay Soils, Wageningen,
Neth. ILR Pubn. 37, 89–100, 1985.
Beven, K. J. and Germann, P. F.: Macropores and water flow in soils
revisited, Water Resour. Res., 49, 3071–3092, https://doi.org/10.1002/wrcr.20156, 2013.
Germann, P. F. and Beven, K. J.: Water flow in soil macropores, I. An
experimental approach, J. Soil Sci., 32, 1–13, 1981a.
Germann, P. F. and Beven, K. J.: Water flow in soil macropores, III. A
statistical approach, J. Soil Sci., 32, 29–31, 1981b.
Germann, P. F.: Preferential Flow: Stokes approach to infiltration and drainage, University of Bern Press, available at: https://boris.unibe.ch/119081/1/preferential_flow.pdf (last access: 1 March 2021), 2014.
Why does water know/where to flow?/Is the strongest force/dictating the course?/Is the weakest resistance/controlling the distance?/Or is soil hydrology nothing but mental strength/fiddling with mass, time, and length?
The success of terrestrial plants relies, among other phenomena, on the simultaneous supply of oxygen and water to the root tips in the size range of <5 to >50 µm. A mandatory prerequisite is the inferior water pressure relative to the air pressure around the tips. That again is the result of the water's surface tension against the air and its affinity towards the solid particles, resulting in the capillary potential ψ. As a physicist with the US Bureau of Soils, Lyman Briggs (1897) formalized the relationships mathematically and physically. He made use of data from a sand column experiment, reported in Franklin King (1892), 42 in. (1.067 m) high, that was completely water saturated and then left to drain for 40 d. He qualitatively expressed an equilibrium between the gravitational and capillary forces, represented by height and pressure drop across the water meniscus, deducing that moisture content will decrease with height in the column.
Briggs also provides a qualitative description for flow when there is any deviation from this static equilibrium in terms of a capillary gradient and further postulated a variable permeability concept in partially water-saturated soils. He certainly introduced these concepts to Edgar Buckingham, who joined the Bureau of Soils to work under Briggs in 1902. Buckingham further developed these concepts, and his reports on the movement of soil moisture are frequently viewed as the origin of modern concepts of capillary flow (Buckingham, 1904, 1907): he extended a first-order gradient flux law to unsaturated soils as analogous to thermal and electrical fluxes (though does not explicitly mention Darcy's law), and he proposed hydraulic conductivity, diffusivity and the water capacity as quantitative functions of soil moisture. However, “Buckingham did not manage to formulate a clear-cut physical-mathematical flow theory that quickly inspired other soil physicists” (Raats and Knight, 2018, p. 11).
This seminal work at the Bureau of Soils was set back by the Chief of the Bureau, Milton Whitney (who was chief from 1860 to his retirement in 1927). Whitney dismissed King in 1904 because of his belief that soil nutrient status was more important to crop growth than the soil physical properties favoured by Whitney. He also encouraged Briggs to leave in 1905 because his training as a physicist was resulting in the application of “rigid mathematical demonstration” to soil physics that Whitney felt could not be justified (see Landa and Nimmo, 2003). After the departure of Briggs, Buckingham worked under Frank Kenneth Cameron, who was not totally convinced by Buckingham's developments, suggesting that there might be inconsistencies in Buckingham's approach to water and vapour transport. Buckingham's response was not totally convincing, but Cameron decided not to hold back the publication as “you seem to be convinced that it is all sound and safe” (quoted in Nimmo and Landa, 2005). Buckingham's 1907 report was delayed as a consequence until after he had also left the Bureau of Soils to join the National Bureau of Standards in August 1906. He never returned to the study of soil physics. He became much better known as the author of the Π theorem for dimensional analysis (Buckingham, 1914), which was only much later applied to soil moisture characteristics (e.g. Miller and Miller, 1956).
It was more than two decades before there was further significant progress with Lorenzo K. Richards' (1931) paper “Capillary Conduction of Liquids Through Porous Mediums”, where he presented the three-dimensional form of the second-order convection–diffusion equation, which bears his name. Note that, despite the comment of Raats and Knight (2018) quoted above, all the elements of the Richards equation were already present in the report of Buckingham (1907), but there he did not combine them into a single flow equation. In fact, Richardson (1922) had already done so before Richards but outside the context of the soil physics community (see Raats and Knight, 2018). Richards did, however, also present an experimental procedure for the determination of the parameters of his equation, including a demonstration of hysteresis in the soil water characteristics. This combination of theory and experiment based on that experiment made the approach attractive for practical applications.
However, Richards was also instrumental in introducing some misconceptions into soil physics. He authoritatively stated the following:
If there is a steady flow of liquid through a porous medium which is only partially saturated, then the larger pore space containing air and the effective cross-sectional area of the water conducting region is reduced. If these air spaces could in some way be filled with solid, the condition of the flow would be unchanged and the proportionality between the flow and the water-moving force would still hold because Darcey's [sic] law is independent of the size of particles or the state of packing.
(Richards, 1931, p. 323)
This statement reveals the fundamental, but scientifically quite wrong, exclusivity he put on capillarity-driven flow during infiltration. Since then it has been raised to a soil hydrological dogma that we are still confronted with today. In the theory of Richards, increasing the flow rate in a partially saturated porous medium mandatorily requires the increase of the hydraulic gradient by locally either increasing or decreasing capillary potential that, in turn, has to equilibrate in either case with the water content. In Richards' context this is only feasible during infiltration when flow remains sequential: finer pores have to fill before coarser pores are allowed to (Germann, 2018a, b). Indeed, it has been suggested that the Richards' experiment, which relied on the application of air pressure to ensure that the larger pores were empty at each potential and flow rate, was simply the wrong experiment for flows under more natural conditions (Beven, 2014, 2018).
A reconsideration of the ubiquity of Richards' (1931) capillary approach to infiltration and drainage demands a concept that replaces this assumption of dominance by capillarity. In early attempts, Germann and Beven (1981), Beven and Germann (1981), and Germann (1985) successfully approached transient infiltration/drainage with kinematic wave theory that can be applied when gravity is the dominant driving force rather than the gradient of capillary potential, which will be the strongest driver under drier conditions. More recently, Germann and al Hagrey (2008) summarize the features of gravity-dominated viscous film flow1 during transient infiltration and drainage in the Kiel sand tank: (i) constant velocity of the wetting front, (ii) collapse to atmospheric pressure of capillarity behind the wetting front, and (iii) infiltration and drainage follow the same simple rules of viscous film flow. Moreover, no pore classification or size distribution or consideration of heterogeneity of soil properties is required for the application of viscous film flow, since film thickness, flow velocity, and celerity during both wetting and drying can be related to flux rates.
Infiltration expresses how water arriving from above the ground, usually in the shape of drops, transitions to water flow in the soil below the ground surface. Drops have internal pressures higher than atmospheric pressure. According to Laplace–Young theory, pressures against the atmosphere in drops increase from about 15 to 750 Pa as their diameters reduce from 5 to 0.1 mm. When drops hit the ground surface, depending on their size and Bond number, they will often burst. The remnants then join and form local films at atmospheric pressure. There are two ways for water to continue. Either water has to follow the strongest gradient, as in capillary flow. Richards' (1931) forceful conjecture of the dominance of capillarity during infiltration in unsaturated porous media works well under steady-state conditions. However, increasing the flow rate causes the well-known phenomena of non-equilibrium flow, macropore flow, and preferential flow. Water then follows the way of least resistance, as a viscous film flow. This type of flow occurs under atmospheric pressure, regardless of the thickness and path widths of the films, as Flammer et al. (2001) have demonstrated with acoustic velocity measurements across soil columns. Germann (2018b) also demonstrates how acoustic velocity experiments suggest that preferential flows can proceed faster than capillary gradient-driven fluxes in unsaturated soils.
On the one hand, the Richards' (1931) capillary gradient flow (and implied local equilibration of potentials) continues to be taught and used in models of soil hydrology in a rather dogmatic way. There have been modifications suggested to allow for dual permeability functions near saturation, but these are not really convincing (Beven and Germann, 2013; Beven, 2018). On the other hand, there are a plethora of review articles that discuss the hydro-mechanical inconsistencies with the Richards equation and observations of preferential, non-equilibrium, and macropore flows in both unsaturated and saturated soils (see again Beven, 2018, and references therein). This conflict remains to be resolved but is clearly important for the understanding of both flow and transport. It is, however, the case that there are few ongoing research efforts, either theoretical and experimental, on developing coherent descriptions of preferential flow in soil physics. The author's application of viscous film flow concepts to infiltration in unsaturated soils has been one such effort, and it is hoped that it will be taken on and further developed by others (see, for example, the recent papers of Germann, 2017, 2018a, b; Germann and Prasuhn, 2018; Germann and Karlen, 2016).
In conclusion, Briggs' (1897) convenient and, within his concept, correct definition of capillary flow led, via the work of Buckingham, to Richards' (1931) dogma of the unproven dominance of capillary gradient-driven fluxes during infiltration that is still widely used today. However, as it turns out, while capillary flow relies on the strongest force exerted on water in an unsaturated soil, the weaker force of viscosity can dominate during infiltration as a result of the formation of film flows at and near the soil surface.
I was shocked and deeply saddened to learn, after I had written my review of his paper, that Peter Germann had died. When Erwin Zehe last fall invited me to review this paper for HESS, I was delighted, and I wrote it in anticipation of a spirited in-print discussion with Peter, which sadly will not happen. Now I am pleased to see that Keith Beven has written an impressive revision of Peter's manuscript.
The missed opportunity for discussion of this paper is a small part of the loss I feel in Peter's death. He was a tremendous inspiration to me, ever since he warmly befriended me at an AGU meeting years ago. Peter enlightened me with his profound insights. Moreover, he encouraged and energized me by his bold example in putting forth innovative, even revolutionary, ideas into a scientific realm where they were needed and fruitful. Though in person he is no longer with us, his many written works will continue to enlighten and inspire scientists into the future.
No data sets were used in this article.
This article is part of the special issue “History of hydrology” (HESS/HGSS inter-journal SI). It is not associated with a conference.
This paper was edited by Erwin Zehe and reviewed by John R. Nimmo.
Beven, K. J.: BHS Penman Lecture: “Here we have a system in which liquid water is moving; let's just get at the physics of it” (Penman 1965), Hydrol. Res., 45, 727–736, https://doi.org/10.2166/nh.2014.130, 2014.
Beven, K. J.: A century of denial: Preferential and nonequilibrium water flow in soils 1864–1984, Vadose Zone J., 17, 180153, https://doi.org/10.2136/vzj2018.08.0153, 2018.
Beven, K. J. and Germann, P. F.: Macropores and water flow in soils revisited, Water Resour. Res., 49, 3071–3092, https://doi.org/10.1002/wrcr.20156, 2013.
Briggs, L. J.: The mechanics of soil moisture. Bulletin No. 10, U.S. Department of Agriculture, Division of Soils, Washington, DC, 1897.
Buckingham, E.: Contributions to our knowledge of the aeration ity of of soils, Bulletin 25, USDA Bureau of Soils, Washington, DC, 1904.
Buckingham, E.: Studies on the movement of soil moisture, U.S. Department of Agriculture, Bureau of Soils, Bulletin No. 38, Washington, DC, 1907.
Buckingham, E.: On physically similar systems; Illustrations of the use of dimensional equation, Phys. Rev., 4, 345–376, 1914.
Flammer, I., Blum, A., Leiser, A., and Germann, P.: Acoustic assessment of flow patterns in unsaturated soil, J. Appl. Geophys., 46, 115–128, 2001.
Germann, P. F.: Kinematic wave approach to infiltration and drainage into and from soil macropores, Trans. ASAE, 28, 745–749, 1985.
Germann, P. F.: Preferential flow – Stokes approach to infiltration and drainage. Geographica Bernensia, Bern (Switzerland), 199 p., available at: https://boris.unibe.ch/119081/1/preferential_flow.pdf (last access: 1 March 2021), 2014.
Germann, P. F.: Shape of Time Domain Reflectometry Signals during the Passing of Wetting Fronts, Vadose Zone J., 16, 1–5, 2017.
Germann, P. F.: Viscosity – the weak link between Darcy's law and Richards' (1931) capillary flow, Hydrol. Process., 32, 1166–1172, 2018a.
Germann, P. F.: Hydromechanics and kinematics in preferential flow, Soil Sci., 183, 1–10, 2018b.
Germann, P. F. and al Hagrey, S. A.: Gravity-driven and viscosity-dominated infiltration in a full-scale sand model, Vadose Zone J., 7, 1160–1169, https://doi.org/10.2136/vzj2007.0172, 2008.
Germann, P. F. and Karlen, M.: Viscous-flow approach to in situ infiltration and in vitro saturated hydraulic conductivity determination, Vadose Zone J., 15, 1–15, 2016.
Germann, P. F. and Prasuhn, V.: Viscous flow approach to rapid infiltration and drainage in a weighing lysimeter, Vadose Zone J., 17, 1–12, 2018.
King, F. H.: Fluctuations in the Level and Rate of Movement to Ground Water, U.S. Dept. of Agriculture, Bureau of Soils, Bulletin. No. 5, 25 pp., Washington, DC, 1892.
Landa, E. R. and Nimmo, J. R.: The life and scientific contributions of Lyman J. Briggs, Soil Sci. Soc. Am. J., 67, 681–693, 2003.
Miller, E. E. and Miller, R. D.: Physical theory for capillary flow, J. Appl. Phys., 27, 324–332, 1956.
Nimmo, J. R. and Landa, E. R.: The soil physics contributions of Edgar Buckingham, Soil Sci. Soc. Am. J., 69, 328–342, 2005.
Raats, P. C. A. and Knight, J.: The contributions of Lewis Fry Richardson to drainage theory, soil physics, and the soil-plant-atmosphere continuum, Front. Environ. Sci., 6, 13, https://doi.org/10.3389/fenvs.2018.00013, 2018.
Richards, L. A.: Capillary conduction of liquids through porous mediums, Physics, 1, 318–333, 1931.
Richardson, L. F.: Weather Prediction by Numerical Process, Cambridge University Press, Cambridge, UK, 262 pp., 1922.
John Nimmo in his comments on this paper (see https://hess.copernicus.org/preprints/hess-2020-499/) points out that there is problem in Peter Germann's use of “viscous flow” to describe his film flow concepts since viscosity is intrinsic to all types of flow, including flows that conform to the Buckingham–Richards theory, where viscosity is intrinsic to the definition of hydraulic conductivity; however it often does not appear explicitly in expositions of the Richards equation. Viscosity does appear explicitly in the Stokes relations for gravity-dominated film flows. In editing the paper Keith Beven has therefore referred to viscous film flow to keep continuity with Peter's usage.