Micropiping processes and biancana evolution in southeast Tuscany, Italy

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Geomorphology20 (1997) 219-235

Micropiping processes and biancana evolution in southeast Tuscany, Italy Dino Torri a, *, Rorke B r y a n b a C.N.R.-I.G.E.S., Piazzale delle Cascine 15, 1-50144 Firenze, Italy b Soil Erosion Laboratory, University of Toronto (Scarborough), 1265, Military Trail, Scarborough, Ont. M1C 1A4, Canada

Received 15 January 1995; accepted 15 August 1995

Abstract Biancane badlands consisting of small domes dissected by rills and micropipes, with rough disordered microrelief, can be found along the Apennines in Italy. The dominant processes forming biancane differ from those of badlands formed on smectite-rich mudrocks, as micropipes associated with pseudokarstic enlargement of pores and cracks predominate and form the main routes for evacuation of eroded material. Biancana evolution is controlled by water infiltration into intact bedrock, producing an erodible weathering 'rind' which is more porous than intact rock. This rind is easily removed by rill or micropipe flow, and erosion is therefore 'weathering-controlled', depending on rind production by infiltrating water. Infiltration is initially slow and stepped, due to slow water movement through very small capillary pores in intact rock alternating with rapid filling of macropores and cracks. This occurs due to rapid matrix pore enlargement by dispersion and/or dissolution. The infiltration pattern is accurately reproduced by a model built on progressive development of weathering layers by moisture penetration. Model results are consistent with weathering rind depths and erosion observed in the field, and show that a pipe network can be generated on newly exposed rock by the rainfall of one year. Propagation of the pipe network diverts a progressively larger proportion of runoff into micropipes, expanding weathering rind production within the biancana as well as on the surface. Internal weathering and flow progressively dominate with few unweathered corestones, and the biancana gradually collapses into a penultimate 'souffle-like' form. © 1997 Elsevier Science B.V. Keywords: badlands; erosion; weathering; piping; infiltration

I. Introduction Badland landforrns occur along much of the length of the Apennine c!hain in Italy. Many landforms resemble those in badlands elsewhere (Marinelli,

* Corresponding author. Fax: +39 55 321148; E-mail: [email protected]

1915) but two characteristic landforms known as 'calanchi' and 'biancane' are also common. These features sometimes form separately (e.g., in Tuscany, Vittorini, 1977), apparently reflecting differences in material clay content, mineralogy and cation adsorption characteristics, but in other areas differences are less clear and transitional forms have been identified (e.g., in Basilicata, Alexander, 1982).

0169-555X/97/$17.00 c~ 1997 Elsevier Science B.V. All rights reserved. PH S0169-555X(97)00025-1

220

D. Torri, R. Bryan / Geomorphology 20 (1997) 219-235

The precise relationships between calanchi and biancane have engendered much discussion, and characteristics and material properties have been described in several papers (e.g., Vittorini, 1977; Guasparri, 1978; Alexander, 1980, 1982; Pinna and Vittorini, 1989; Rodolfi, 1991). Calanchi are usually much larger landforms with well-developed drainage networks formed by surface processes, especially rillwash, gullying and frequent shallow landsliding on very steep slopes. Piping is limited and usually confined to mudflow materials, though Alexander (1980) has identified cavitation piping along tension cracks in material in situ. Biancane are small clay domes, up to 20 m in height, which typically occur in clusters. They are dominated by incised rills and micropipes developed in bedrock, and are surrounded by miniature pediments. Calanchi and biancane have frequently been described, but there have been few detailed process studies, and understanding of their formation is limited, particularly in the case of biancane. Calanco development appears active in many parts of Italy and the total area of calanchi is probably expanding. By contrast, the smaller biancane are easily disturbed by agricultural operations, and have been greatly reduced in extent in recent years by slope levelling with bulldozers (Bigi et al., 1988). Biancane resemble some landforms in other clayrich badlands (Bryan and Yair, 1982), but it is not clear that either formation processes or landforms are identical. Most information on clay badland processes has come from smectite-rich lithologies in arid or semiarid areas (Schumm, 1956; Yair et al., 1980; Bryan and Hodges, 1984) where intense shrink-swell activity often produces relatively deep, loose, 'popcorn' regolith ( > 0.3 m) of high macroporosity (Imeson, 1986; Finlayson et al., 1987). Complex, three-dimensional micropipe systems develop in this regolith which control rill network evolution and hillslope erosional response (Bryan et al., 1978; Hodges and Bryan, 1982; Bryan and Harvey, 1985; Gerits et al., 1987). The geometry of rill and micropipe systems is apparently controlled initially by desiccation cracks, though linkage between dominant rill and pipe spacing and established drain-spacing criteria has been suggested by Gerits et al. (1987) and Imeson and Verstraten (1988). By contrast, biancane develop on Pliocene marine

clays throughout Italy in quite varied climatic conditions. In some parts desiccation is much less intense and the disrupted 'popcorn' regolith is often much thinner. The Apennine chain has been intensely disturbed by frequent tectonic activity resulting in abundant complex fracturing. Where highly porous regolith is not well-developed, the rill and micropipe formation and biancane evolution is apparently strongly influenced by the characteristics of these tectonic lineations. The present study was undertaken in a residual area of biancane in southeast Tuscany to identify the origins of micropiping and its influence on biancane evolution.

2. Study site and design The experimental site is located at Podere Beccanello, in Val D'Orcia, part of a larger landholding known as La Foce-Chiarentana (Fig. 1). Biancane have developed in marine clays laid down in the structural Radicofani Basin during the Early and middle Pliocene, and uplifted during the Pleistocene (Losacco, 1963). The area was strongly influenced by subsequent tectonic disturbances which affected all of southern Tuscany, producing a complex pattern of tectonic lineations which have been linked with landslide initiation (Alexander and Formichi, 1993). At Podere Beccanello, two sets of vertical or subvertical joints traverse the biancana zone, with trends of N100 and N60 (Fig. 1), producing a dense rhomboidal net of fractures with oxidized bands about 0.1 m in width (Colica and Guasparri, 1990). Some of these fractures are 10-15 m in depth. The Beccanello biancane were initially part of an extensive biancana development on a SW-facing 10° slope. Only residual undisturbed patches, like the 15 ha Beccanello site, still exist. Individual biancana vary in size, but are typically about 20 m in diameter and 5-8 m in height, producing a cluster of rather regular size and spacing (Fig. 2). Biancane are usually asymmetrical with steeper bare south-facing slopes (up to 60 °, but typically 30-40°), while northern slopes are 20-30 ° and usually covered in vegetation. South-facing slopes are active erosional bedrock surfaces with a thin (5-15 cm) regolith, and are deeply dissected by rill channels, micropipes and

D. Torri, R. Bryan / Geomorphology 20 (1997) 219-235

occasional slump scars. Vegetation on north-facing slopes is dominated by Bromus erectus (Calzolari et al., 1993a), often with Spartium junceum shrubs with well-developed soils up to 1 m deep on more stable slopes (Calzolari et al., 1993b). Both slopes are flanked by low-angle (1-2 °) depositional micropediments where sheetwash occurs during more intense rainstorms. Biancane maintain their typical form until an advanced stage of development, when they assume a 'soufflr-like' form (Fig. 3a) in which largely unweathered corestones (Fig. 3b) are separated by extensive weathering and piping along fracture planes. Material propertie:~ of the marine clays at Becca-

nello are shown in Table 1. The Beccanello data include the biancane material proper (B), the thin oxidized fractures described by Colica and Guasparri (1990), (F) and the basal micropediment. Textures of biancane and fracture material are almost identical, with slight evidence of selective removal of fine silt from the fracture. The micropediment data show strong selective deposition of sand and silt. Data for the weathered regolith crusts and underlying intact rock suggest very slight selective removal of clays from the surface. Clay minerals are dominated by quartz, calcite and smectite, with low to moderate plasticity, and bulk densities are 2.15 g cm -3 and 1.8 g cm -3 for bedrock and regolith crust, respec[]

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Fig. 1. Map showing the location of La Foee-Chiarentana, and detailed site map of Podere Beccanello (modified after Colica and Guasparri, 1990). Lines represent joints, ellipsoids represent biancane.

222

D. Torri, R. Bryan/Geomorphology 20 (1997) 219-235

tively. Plasticity, shrinkage, and crust bulk density are similar to the Guadix badlands in Andalucia, where the clay content is much lower (Gerits et al., 1987), but they are much lower and higher, respectively, than the clay and smectite-rich Alberta badlands in Canada (Hodges and Bryan, 1982). Soluble salts are abundant with a Na concentration of 0.20.4% by weight (Torri and Monaci, 1991), which is reflected in high SAR and EC values. There are two local long-term climatic stations, at Spedaletto (8.5 km to the west-northwes0 and La Foce (2.5 km to the north-northeas0, supplemented since 1990 by a weather station at Podere Beccanello (Fig. 1). The climate is transitional between subhumid and sub-arid, with a summer moisture deficit at Spedaletto, but not at La Foce. Average annual precipitation (1951-1980) is 675 nun for Spedaletto and 815 mm for La Foce, with maxima at both stations in autumn and minima in July-August (Calzolari et al., 1993b). Some snow occurs in most

winters, but seldom persists for more than a few days. Mean rainfall (1991 and 1992) is 645 mm for Beccanello, with an average of 118.5 raindays, and a total of 41.25 m m for the three rainiest days. The limited available rainfall i n t e n s i t y - d u r a t i o n frequency data are summarized in Table 2. Few data are available on biancane erosion rates. Raglione et al. (1980) measured annual sediment loss of 17.5 kg m -2 with runoff troughs in Calabria, equivalent to denudation of 14 mm a -l. Alexander (1982) measured denudation ranging from 17 to 57 mm a - l with erosion pins in Basilicata, and in the Beccanello biancane, Colica (1992) measured denudation rates equivalent to 36 mm a -1. These data summarize erosion rates but provide little information about the precise processes involved. In two brief sprinkling tests on a Beccanello biancana T o m et al. (1994) found detectable runoff only in rills and micropipes, with detachment-controlled sediment release reaching a peak concentration of 160 g 1-~ in

Fig. 2. Characteristicbiancanadome clusters at Beccanello.

D. Torri, R. Bryan / Geomorphology 20 (1997) 219-235

Fig. 3. (a) Penultimate 'souffle-like' stage of biancana evolution. (b) Residual corestone in intensely weathered penultimate biancana.

223

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D. Torri, R. Bryan/Geomorphology 20 (1997) 219-235

Table 1 Summary of material characteristics of unweathered rock on south-facing biancana slopes at Podere Beccanello Particle size (mm) < 0.002 B F Pd

0.002-0.020

0.02-0.05

0.05-2

mean

range

mean

range

mean

range

mean

range

46 48 20

40-50 45-50 15-25

44 42 55

40-48 40-45 49-57

8 8 20

5-14 5-16 13-29

2 2 5.0

1.0-4.0 1.0-4.0 4.0-7.0

P1 (%)

PI

AI

Bulk density (kg m- 3)

Consistency limits

Density and porosity

LL (%) B F

mean

range

mean

range

47 49

45-49 47-52

24 25

23-26 23-26

Saturated pas~ extract B F Pd

23 24

0.5 0.5

mean

range

2150

2000-2300

Modified COLE a

SAR

EC (S m- 1)

moisture (%)

20.5 29 15

11 14 0.5

57 59 40

0.057

B = unweathered rock; F = oxidized band (joints and cracks); Pd = micro-pediment; LL = liquid limit; PL = plastic limit; PI = plasticity index; AI = activity index; SAR = sodium absorption ratio; EC = electrical conductivity; COLE = coefficient of linear expansion. a After Alioto et al. (1989). b After Alioto et al. (1989).

dry antecedent conditions. This agrees well with a peak concentration o f 149.6 g 1-1 m e a s u r e d b y Sorriso-Valvo et al. (1995) in a m o r e p r o l o n g e d test at similar rainfall intensity o n a Calabrian b i a n c a n a slope. Torri et al. (1994) measured highest water and sediment discharge in micropipes, but because of the complex, d y n a m i c b e h a v i o u r o f micropipes, precise drainage area or v o l u m e could not be established. It is therefore difficult to compare erosion rates with the denudation rates cited. It is, however, clear that

Table 2 Summary rainfall duration, mean maximum intensity and frequency data for Podere Beccanello (1991) and Podere Beccanello (1992) Duration (min)

Mean max. intensity (mm h - 1)

2-year frequency (No.)

60 30 10

14.5 20.3 41.5

5 10 5

m u c h erosion is sub-surface, and denudation rates measured from erosion pins alone m u s t considerably underestimate actual erosion rates. The sprinkling tests show that in the Beccanello b i a n c a n e m u c h flow is routed through and erosion concentrated in micropipes. The influence of pipes, once opened, o n infiltration and throughflow patterns is obvious, but the precise processes i n v o l v e d in pipe d e v e l o p m e n t are not. It seems that it must be related to localised infiltration along tectonic fractures, but p o n d i n g tests o n bedrock stripped of regolith showed no clear difference b e t w e e n oxidized fractures and unfractured bedrock. The object of this study was to explain the process o f micropipe evolution by: (1) m e a s u r e m e n t of rill and micropipe characteristics on representative biancane, and identification o f any apparent relationship to tectonic fracture patterns; (2) laboratory tests of b i a n c a n a fragments u n d e r rainfall; (3) d e v e l o p m e n t of a m o d e l to describe micropipe d e v e l o p m e n t in rainfall conditions typical of Beccanello.

D. Torri, R. Bryan/ Geomorphology20 (1997) 219-235

3. Results 3.1. Rill, micropipe and fracture characteristics on representative biancane

Surface characteristics of six randomly selected biancane were measured on representative 2 m 2 sections located 1 m above the base of bare, south-facing slopes. Observations included spacing and orientation of fills, mlcropipes and oxidized fractures, and regolith characteristics. All surfaces had rough, disordered 'popcorn' regolith, with varied microtopography (Fig. 4). Surface roughness was seldom < 0.01 m, so many small irregular channels were formed by interrill flow around individual 'popcorn' units. These were ignored, fills being arbitrarily defined as more continuous, straight features, incised at least 0.01 m into the surf~tce. Micropipes could be identified only by inlets or outlets, or occasionally by collapsed roof sections. The most significant features were measured, and some were excavated, but some mlcropipes were almost certainly missed.

225

Precise fracture identification and measurement also posed problems. Fractures could be identified primarily by oxidization, but some features were broad (up to 0.1 m width) with clear structural differences, while others were narrow and lacked structural distinction. Some fractures were continuous and straight but others curved, bifurcated and discontinuous. Only fractures which were continuous across measurement sections were measured. Fracture patterns are further confused by what are apparently unloading fractures, particularly near the base of convex slopes. The location and orientation of fractures, rills and micropipes have been plotted on site diagrams in Fig. 5, and summary data are shown in Table 3. Despite filtering microscale features, general relationships are difficult to identify. Some fills coincide with micropipes, but others do not, and the relation to fracture patterns is not obvious either. However, only fills associated with pipes are incised more than 0.015 m below the immediate surrounding surface. These are major fills which traverse the complete sample section, and in most cases the complete

Fig. 4. Typicalbiancanasurfacemicrorelief.

226

D. Torri, R. Bryan/Geomorphology 20 (1997)219-235

Table 3 Summary data for rill and crack occurrence at six representative sites on south-facing biancana surfaces Site

1 2 3 4 5 6

Slope

Orientation

Shape

Curvature

(°)

(°)

(°)

(°)

51 50 47 44 44 44

150 192 160 205 120 130

Straight Convex Straight Convex Concave Concave

na 16 na 15 30 105

Regolith depth

' Vertical cracks'

'Horizontal

interrill (m)

rill (m)

orientation (°)

spacing (m)

orientation (°)

cracks' spacing (m)

Rills orientation (°)

spacing (m)

0.083 0.064 0.048 0.041 0.030 0.028

0.012 0.005 0.036 0.008 0.013 0.020

79 82 59 99 75 80

0.54 > 0.65 1.0 > 0.80 0.63 0.65

8 3.5 16 4 1 5

0.60 0.28 > 1.0 > 0.80 0.48 1.0

88 89 87 86 91 95

0.42 0.31 0.23 0.40 0.34 0.20

excavated pipes is frequently > 0.07 m below the surface. The orientation of dominant rill/micropipes generally reflects overall slope shape, being parallel on straight biancane (Sites 1, 3), slightly divergent on convex biancane (Sites 2, 4) and convergent on concave biancane (Sites 5, 6). The average orienta-

biancana slope. Some are exposed rill channels, but most are discontinuous with intervening micropipe sections above which rill incision is much less pronounced. Micropipes are typically 0.03-0.04 m in diameter, with roofs 0.03-0.04 m thick, and thalwegs approximately parallel to the slope surface. Depth of pipe development is highly variable, but in

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D. Torri, R. Bryan/ Geomorphology 20 (1997) 219-235

tion for all fills is 89°, nearly parallel to the steepest slope. Detailed fill orientation is also strongly affected by mesoscale slope topography. Shallow, non-piped rills ( < 0.0115 m depth) are usually located on 'interrills' between deeper, piped rills, which are typically incised into the base of broad 'swales.' On smaller biancane (Sites 1, 2) these are up to 0.15 m wide and incised 0.12, m below the general surface, while on larger bianc~aae (e.g., Site 5), they can be 1 m wide and 0.75 m below the general surface. Once

227

formed, these 'swales' can concentrate water towards rill/micropipe channels. The relationship between the major rill/micropipe channels and fracture patterns is not obvious. Some rills coincide with fractures, but the average orientation of 'vertical' fractures is 67 °, cutting obliquely across rill channels. Even considering only major fills, average spacing is less than half average fracture spacing. As noted, the most significant fills are associated with pipes, but excavation of domi-

Fig. 6. Excavationof a diagonalpipe channel, developedalong a fracture.

228

D. Torri, R. Bryan / Geomorphology 20 (1997)219-235

nant rill/micropipe systems, for example at Sites 3, 5 and 6, shows deeper pipe systems (up to 0.25 m) developed along major fractures, diagonally across surface drainage lines (Fig. 6). Some showed a distinct zig-zag course, with alternating sections of varying length straight downslope and obliquely along fractures. These deeper pipe systems are narrow (0.3-0.4 m), with irregular thalwegs. Most crack pipes show evidence of significant flow, such as clay deposition, and can clearly concentrate much of the flow from a biancana slope. No fractures blocked entirely by clay deposition were observed, though this could happen in shallow fracture systems during prolonged rainfall. Biancana surfaces at Beccanello superficially resemble highly active 'popcorn' surfaces on sodic smectites in western Canada and Kenya (Bryan et al., 1988), but the detailed structure is quite different, with shallower regolith and lower desiccation crack (as distinct from tectonic fracture) density. This reflects lower clay contents and less active clays. Nevertheless, weathering produces a highly erodible surface 'rind' which can be easily entrained to produce high sediment loads (Torri et al., 1994). Surface removal is concentrated in rills, as suggested by average regolith depths of 0.049 and 0.016 m for interrills and rills, respectively. In some fills 'rind' depth is only a few millimetres and it can be easily stripped by rill flow during rainstorms. Torri et al. (1994) confirm this 'weathering-limited' removal, with peak rill sediment discharges during initial flow. The rind is restored by moisture-controlled weathering between runoff-producing storms, so peak rill sediment concentrations during storms should be controlled by the rapidity of weathering and the number of wetting/drying cycles between runoffproducing storms. While rill erosion can significantly affect biancana development, Torri et al. (1994) found highest sediment discharge from pipes, and the factors controlling flow routing through pipes are therefore critical. Site observations suggest close correlation between pipe and fracture development. Where fractures are open, as with unloading fractures, water

obviously penetrates easily and leads to internal regolith weathering. The first development of the more frequent oxidised tectonic fractures is less clear. Newly excavated oxidised fractures are closed, but typically show denser cleavage and fracturing than the surrounding matrix and slightly higher SAR values (Tables 1 and 2). On some surfaces oxidised areas are less resistant and form depressions, but this is not consistent. The denser cleavage could be expected to result in preferential infiltration, but comparative ring infiltrometer tests on horizontal surfaces cleared of regolith in the field did not support this conclusively. The key factors affecting biancana development are the pattern of regolith development by wetting, the processes leading to concentrated infiltration and the development of piping. Laboratory experiments were carried out with biancana samples to provide further information on both processes. 3.2. Laboratory experiments

Two laboratory experiments were carried out. In the first, ring infiltrometer experiments were carried out on intact blocks of biancana material, 0.07-0.09 m in diameter and 0.03-0.05 m in thickness. Upper surfaces were planed off, and 0.05 m diameter ring infiltrometers were sealed to the surface with silicon, which was also used to cover the remainder of the upper surfaces. Samples were placed on a sand bed for stability, so that water could drain either laterally or through the base. Water was added to the infiltrometer to keep the water level essentially constant. Four tests were run: two with residual small shard blocks from the weathered regolith, one with an intact rock fragment carved from the core of a 0.3 m 3 block, and one from a block of intermediate size. It was not possible to obtain an intact block with an oxidized crack. The results of infiltration tests (Fig. 7a,b) show much higher initial infiltration rates on weathered 'rind' samples (4.8 and 46.2 mm h - 1 during the first 15 min) compared with 1.2 mm h -1 for the core sample. Data for the intermediate sample were dis-

Fig. 7. (a) Initial cumulative infiltration in laboratory ring infiltrometer tests weathered samples and intact rock. (b) Complete ring infiltrometer cumulativeinfiltration curves. (c) Cumulativeinfiltration on intact corestone showing characteristic steppedpattern.

D. Torri, R. Bryan/Geomorphology 20 (1997) 219-235

229

(a) 22 WEATH~ED

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120

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180

Time (min)

(b) 24

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200

250

I 1440

1600

230

D. Torri, R. Bryan/Geomorphology 20 (1997) 219-235

torted by major cracking and are not included. Weathering associated with moisture penetration transforms the material, progressively increasing moisture penetration in subsequent storms. However, this effect is somewhat time-dependent, as shown by the decline in rate on the regolith sample with the highest initial rate after 21 min to a sustained rate similar to that for the unweathered core sample. This suggests that moisture in the regolith sample had penetrated to an unweathered core. The last stage of each test was very rapid infiltration (shown for the core sample, Fig. 7b) precluding precise measurement, which just preceded exfiltration of water from the sides and base of the sample, and sample collapse in a mudflow. Infiltration into all samples is conspicuously stepped, as shown by the plot of actual corestone sample values over the first 200 min (Fig. 7c). This pattern can only be explained by material in which infrequent large pores or microcracks are separated by intact matrix with very small capillary pores. Water penetration initially driven by capillary tension will eventually reach cracks, bedding planes or macropores, but the rate of gravitational filling will be limited by the extremely small capillary pores of the intact matrix. The key factor in infiltration is interaction of moisture with the material resulting in rapid enlargement of capillary pores, thereby permitting gravitational filling of macropores, and renewed capillary movement once the wetting front reaches intact material. Capillary pore enlargement has been observed at the surface in the field during wetting by fog. The precise process has not yet been fully examined experimentally, but it involves slaking, some differential swelling, dispersion and solution of salt crystals in the matrix. Once infiltration ceases, residual moisture moves towards the evaporating surface, depositing salt crystals and clogging pores near the surface. These crystals initially will tend to impede infiltration during subsequent rainstorms, but are apparently rapidly removed by solution and mechanical erosion of the surface layer.

The infiltration curves in Fig. 7a,b can be interpolated with a Philip-type equation: i = at °5 + bt

where i = cumulative infiltration, t = time, and a and b are constants. The following values were obtained for the corestone block and weathered sample B:

Sample B Corestone

a

b

r 2

0.02 0.01

0.005 0.0005

0.95 0.99

These values are used below in the section on model development. The curve for weathered sample A could not be interpolated due to the small number of observations and strong initial curvature. In the second experiment a large unweathered corestone, obtained from the advanced biancana shown in Fig. 3, was subjected to simulated rainfall in 28 rainstorms over a 23-day period. Mean rainfall intensity was 50.4 mm h-1 and duration for the first 20 storms was 15 rain, thereafter increasing to 45 min, 90 min and finally 120 min. The interval between storms ranged from 1.25 to 73 h, with a mean interval of 21.13 h. The stages in block weathering and progressive development of superficial and deep-seated cracks, resulting in block failure, can be seen in Fig. 8. By the 27th storm, the appearance of the block is essentially indistinguishable from a typical biancana surface at Beccanello. The laboratory experiments described provide considerable insight on the rapidity of regolith weathering and its effect on infiltration and development of micropiping at Beccanello. Initial infiltration rates into unweathered material are very low, reflecting the low porosity, high bulk density and very small pore radii of the material. Infiltration rates may be somewhat higher in the oxidized material, but no data are available. Infiltration is characteristically stepped for reasons discussed above, but the infiltration rate increases rapidly when the wetting front approaches a free face. This can be explained by an

Fig. 8. (a) Laboratorysprinkling test on intact corestone: initial state. (b) Laboratorysprinklingtest on intact corestone: after two rainstorms; cumulative rainfall 27.1 mm. (c) Laboratory sprinkling test on intact corestone: after six rainstorms; cumulative rainfall 77.3 mm. (d) Laboratory sprinkling test on intact corestone: after 27 rainstorms; cumulativerainfall 593 mm.

D. Torri, R. Bryan / Geomorphology 20 (1997) 219-235

231

232

D. Torri, R. Bryan/Geomorphology 20 (1997) 219-235

increase in pore diameter by slaking, dispersion and solution, with ejection of released material at the free face. The existence of a free face is important, permitting accelerated removal of material from pores. The initial development in intact material is probably very slow, but as a dense network of macropores and cracks progressively develops it will accelerate, particularly once significant flow passes through the evolving pipe system. As cracks open, high cleft pore pressures during rainfall will further enhance network development, but otherwise it is cumulative rainfall amount that appears to be more important than rainfall intensity. Ring infiltrometer experiments clearly show higher initial infiltration into weathered regolith surfaces. The total input of water required to bring the test block to a typical field state was 593 mm, approximately equivalent to the mean annual rainfall at Beccanello, but a clearly distinct weathering find was apparent after six rainfall cycles. The threshold rainfall necessary in the field would presumably be somewhat higher as a result of evaporation loss and erosion, although these would differ greatly between internal and external surfaces. 3.3. Model development

Significant information is still required about the precise processes involved in the development of porosity, cracking and piping in rocks of the Beccanello biancane. Nevertheless, the data available from the laboratory experiments permit the development of an initial model of infiltration and weathering on newly exposed biancana rocks. In the model, three dominant processes are described through the following basic algorithms. 3.3.1. Infiltration As noted, data from the laboratory experiments, together with those from field rainfall simulation experiments (Torri et al., 1994) are well described by a Philip-type equation, in which the coefficients of t ( = time since rain initiation) vary in the following ranges:

% = 0.001 to 0.3 c m s - ° 5 Cfin

=

0.00005 tO 0.03 cm S- 1

These coefficients were allowed to increase with

porosity from initial values of Cin 0.0008 cms -°5 and cfin = 0.00004 cm s-1 to reach maxima at a dry bulk density of 1.8 g cm -3. =

3.3.2. Erosion Overland flow was calculated for a water accumulation length of 0.25 m (approximately half the typical distance between successive infiltration 'sinks' (e.g., fractures and fills). Only interrill erosion was considered as a sediment source as data are available from field simulation experiments (Torri et al., 1994, and unpublished data). Following field observations no transport capacity limitation was assumed. Following Torri et al. (1994) runoff detachment was treated as proportional to water penetration depth, but was allowed to decline exponentially over time to 1% of its maximum value, which occurred during initial slaking. 3.3.3. Weathered depth Conceptually, a biancana rock was subdivided in compartments of 0.01 cm thickness, each compartment being characterised by a porosity value which changed with the number of times it was reached by infiltrating water. This was obtained using an Sshaped function:

ag = 1

-

e -n/b

where ag = the aging factor, n = frequency of penetration by infiltrating water, and b = an empirical decay function. Porosity was allowed to change from 0.13 to 0.32, the values observed for corestone and weathered find, respectively. The calculated infiltration amount was redistributed in compartments following porosity, which allowed calculation of the maximum depth reached by the wetting front (md) and the frequency with which water reached each compartment. Finally the eroded depth was subtracted from the maximum depth (md) to yield the residual weathered depth. The model was run for an iteration of 28 rainfall and desiccation cycles. The resulting values for depth of water front penetration are plotted in Fig. 9a, together with measured values derived from the laboratory experiment with the large corestone block. While the fit is not perfect, it is sufficiently close to encourage confidence in the basic logic of the model. The model was then applied to a biancana slope using 10 min interval rainfall data from the Becca-

D. Torri. R. Bryan / Geomorphology 20 (1997) 219-235

a)

, , . m e a s u r e d values 0!

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model forecast

i

BB

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10

15

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(b)

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Elapsed time (days) - - rainaa~mnt ......... cumulativeerosion -- - weatheringdepth waterpercolation

233

nello site for 1991. Following laboratory observations of visible change, the weathered depth was defined as the depth which the wetting front had reached six times. All other parameters were maintained unchanged. The results of this simulation are shown in Fig. 9b. The final weathered depth produced by the model agrees well with measurements for 1989-1991, and 1994, present at three locations where the weathering rind was intentionally removed. Cumulative erosion (Fig. 9c) is also close to the lower limit of the range measured at Beccanello by Colica (1992). The simulation in Fig. 9b not only shows a pattern of weathering and cumulative erosion which matches field observations, but also shows that approximately one year of rainfall can cause enough weathering and erosion to allow water to penetrate a 22 cm thick layer of intact rock and yield 40 m m of cumulative water exfiltration at the base. In fact, such thickness of intact rock are very rarely found at the surface, where cracking reduces intact layers to 2 - 1 0 cm thickness. Consequently, at Beccanello, a well-developed pipe network can easily be generated on newly exposed surfaces with the typical rainfall of one year. Water penetration depth is critical, and the pipe system will develop most rapidly under prolonged low-intensity rainfall, while in short, high storms, surface erosion becomes more dominant. This general pattern is consistent with observations of badland surfaces near Valencia, Spain, where lower annual rainfall and more intense storms result in thinner weathering rind and fewer micropipes (Soriano et al., 1992).

- -

(C)

-~- measurederoai. . . . .

(Collca,1993)

predictedexoslo. . . .

4. Conclusions ,t-

.....

The evolution of the biancane found in many parts of the Apennines is dominated by water move-

.......

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150 200 250 Elapsed time (days)

......................

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#

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300

350

400

Fig. 9. (a) Comparison of modelled and measured water front penetration depths. (b) Results of model simulation using 1991 rainfall data from Podere Beccanello. (c) Comparison between simulated erosion data and erosion pin measurements on wellweathered biancana surfaces at Podere Beccanello by Colica (1992). (Bars are + 1 standard deviation.)

234

D. Torri, R. Bryan/Geomorphology 20 (1997)219-235

ment and erosion along small pipes and micropipes which form rapidly by pseudokarst processes rather than by enlargement of desiccation cracks. Desiccation cracks do occur, but are confined to a thin superficial layer, and apparently have little influence on erosional patterns, Typical small-domed biancana landforms are dissected by straight rills which follow the steepest slope, and numerous pipes and micropipes which follow more erratic courses. Both are erosionally active, but most sediment is evacuated by pipes, and the most deeply incised rills are associated with collapsing pipes. The key process in biancana development is the rapid transformation of the Pliocene marine clay rock on contact with water. Initial infiltration into newly exposed rock surfaces is slow, and characteristically stepped, due to alternation of intact matrix with very small pores and cracked material with macropores. The matrix rapidly changes on contact with water due to slaking, dispersion and dissolution, resulting in rapid formation of a more porous weathering 'rind'. This is easily detached by rill or pipe flow, and has a significantly higher infiltration capacity than intact bedrock. Detached weathering rind material is easily transported and the process rate is 'weathering-limited' by the production rate of the rind. This is controlled by the penetration of infiltrating water, and can be satisfactorily predicted by a model based on infiltration depth and frequency, erosion rates and change in porosity on wetting. Initial biancana erosion is by surface rillwash and shallow micropiping, with most sediment coming from the surface weathering rind. Repeated wetting cycles cause progressive propagation of macropores and enlarged cracks, and progressively deeper water penetration. The model shows that an intact homogeneous 22 cm thick layer of biancana rock will weather and erode sufficiently in one year to allow cumulative water exfiltration at the base of 40 nml. Such thicknesses of intact rock are very rare, as cracks usually reduce the intact layer to 2 - 1 0 cm thickness. Under these conditions extensive shallow piping can easily develop within one year, leading to internal as well as surface weathering rinds. As the biancana evolves, an increasingly large proportion of eroded sediment is generated within the landform, through a pipe network increasingly controlled by tectonic

cracks and bedding planes. The biancana, which is increasingly dominated by enlarged cracks and weathered surfaces, with very few residual corestones, declines to a penultimate 'soufflE-like' feature and eventually disappears.

Acknowledgements The authors wish to thank M. Del Sette for help in conducting some of the tests and in operating the weather station at Beccanello. Thanks are also due to the La Foce-Chiarentana farm for permission to carry out research at Beccanello. R.B. Bryan's participation was supported by research grants from the Natural Sciences and Engineering Research Council, Canada, which is gratefully acknowledged.

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Marinelli, O., 1915. Differences between American and Italian badlands. Memorial Volume of the Transcontinental Excursion of 1912 of the American Geographical Society of New York, New York, pp. 223-230. Pinna, S., Vittorini, S., 1989. Su alcune carratteristiche geotecniche della Valle dell'Era (Toscana), in rapporto alia genesi di calanchi e biancane. Geogr. Fis. Din. Quat. 12, 131-137. Raglione, M., Sfalanga, M., Torri, D., 1980. Misura dell'erosione in un ambiente argilloso della Calabria. Ann. Ist. Sper. Stud. Difesa Suolo, Firenze 11, 159-181. Rodolfi, G., 1991. Forme dei erosione nei sedimenti neogenici e quaterni. In: Mazzanti, R. (Ed.), La Gestione delle Aree Collinari Argillose e Sabbiose. Edizione delle Autonomie, Roma, pp. 19-30. Schumm, S.A., 1956. Evolution of drainage systems and slopes in badlands at Perth Amboy, New Jersey. Bull. Geol. Soc. Am. 67, 597-646. Soriano, M.D., Colica, A., Torri, D., 1992. Estudio preliminar de la influencia de la estructura y propriedas de los materiales en la evolucion de badlands. Estudios de Geomorfologia en Espafia, Actas de la II Reunion National de Badlands, Murcia, pp. 183-191. Sorriso-Valvo, M., Bryan, R.B., Yair, A., Antronico, L., Iovino, F., 1995. Impact of afforestation on hydrological response and sediment production in a small Calabrian catchment. Catena 25, 89-104. Torri, D., Monaci, F., 1991. La meccanica dell'erosione idrica superficiale nei sedimenti neogenici argillosi. In: Mazzanti, R. (Ed.), La Gestione delle Area Collinari Argillose e Sabbiose. Edizione delle Autonomie, Roma, pp. 31-39. Torri, D., Colica, A., Rockwell, D., 1994. Preliminary study of the erosion mechanisms in a biancana badland (Tuscany, Italy). Catena 23 (3-4), 281-294. Vittorini, S., 1977. Osservazioni sulle origini e sul ruolo di due forme di erosione nelle argille: calanchi e biancane. Boll. Soc. Geogr. Ital. Ser. 10, 6, 25-54. Yalr, A., Bryan, R.B., Lavee, H., Adar, E., 1980. Runoff and erosion processes and rates in the Zin Valley badlands, Northem Negev, Israel. Earth Surf. Process. 5, 205-225.