*5.1. Comparison of the Raba River Channel Structure in 1976 and 2015*

Changes in the morphology and functioning of the Raba river channel is presented herein on the basis of a comparison between survey results from 1976 and 2016. Both surveys focused on changes in channel morphology and overall river patterns.

The Raba river channel had already been heavily regulated by the time of the survey study in 1976. However, the regulation structures had not been in place for very long and the channel was still alluvial almost in its entirety. Downcutting had not yet occurred. Narrowing had occurred to a substantial extent. In the 1970s, many semi-natural, multi-threaded reaches were still to be found in the middle section of the Raba River.

In the 1980s and early 1990s, these last semi-natural reaches were finally regulated or became submerged due to the construction of the Dobczyce Reservoir. In addition, the Raba channel became much deeper in the late 1970s and 1980s. This was a natural process that had been accelerated by the effects of river regulation in the Raba channel, gravel extraction from the river bed, limitation of the river free migration zone by railway and road infrastructure, and reduction in the arable land area in the Raba river catchment. This process prompted the Raba River to follow the regulated channel more permanently.

Over the next twenty or so years natural fluvial processes, including major floods, have led to major changes in the morphology of the Raba river channel in comparison with the year 1976.

In 1976, more than 90% of the length of the Raba river channel was alluvial type. The largest number of river reaches were shaped by deposition and redeposition processes as well as lateral erosion in some cases. These reaches occupied 49% of the total length of the Raba River and were characterized by the largest area of bars and large area of undercuts in relation to other reaches of the same river. Downcutting and lateral erosion were detected along 28% of the length of the Raba river channel. In the 1970s, as much as 23% of the river channel consisted of sections with transport function and with levees reinforcing banks (Figure 3).

In 2015, it is difficult to identify one predominant morphodynamic channel type for the Raba river channel in its longitudinal profile. The morphology of the channel is variable and adjusted to local conditions in mountain reaches, and much more homogeneous in basin reaches. The largest number of the river's reaches remain to be shaped by deposition, redeposition, and lateral erosion. Their number is, however, smaller than that in 1976, and they occupy only 36% of the length of the Raba river channel (Figure 3). It is these reaches that contain more than 70% of the area of bars in the entire Raba river channel system. In comparison with 1976, the share of straight sections of river channel has increased to 35% of the length of the channel. This type is present most often in urbanized areas, as well as in regulated reaches and those with levees. Reaches dominated by downcutting and lateral erosion are concentrated in the upper parts of the Raba river channel. These occupy about 30% of the length of the river channel, which is similar to their share from 1976. This type of river channel along with sinuous channels with lateral undercuts includes river reaches featuring rock formations such as rock steps, rock groins, and rock floor. Generally, a river channel of this type is currently rock alluvial in nature. This makes it different from channel reaches identified in 1976 dominated by downcutting and lateral erosion, as they had an alluvial channel floor. Bars present here are not thick and are often deposited directly atop the rocky channel floor.

**Figure 3.** Raba river channel in 1976 and 2015: (**A**) Human impact in the Raba River valley, (**B**) longitudinal profile of the Raba River, (**C**) morphology of the Raba channel in 1976 and 2015, and (**D**) channel types of the Raba River in 1976 and 2015.

This study also examines differences in channel morphologic characteristics for analyzed Raba river channel reaches between 1976 and 2015.

In 2015, the width of the Raba river channel was larger than that in 1976 in more than 75% of the reaches examined. Channel width increased by an average of 14 m, with a maximum increase of 102 m in Channel Reach no. 10 (Figure 4). River bed width increased by 185 m at this site. The width was 45 m after the regulation of the Raba river channel in the 1970s and 1980s and increased to 230 m in 2015 as a result of a few major floods. Spontaneous renaturalization was supported by an artificial supply of gravel to the channel of the Raba River in this river section. This was part of a river restoration project called the "The Upper Raba River Spawning Grounds" [50]; however, the river bed width is still currently lower than the river bed width at the end of the 19th century, in the period before Raba River regulation. River width was ca. 380 m at the time [51].

**Figure 4.** Location of sections undergoing a spontaneous renaturalization in the Raba river channel from 2009 to 2015.

There are some reaches where the channel is narrower than in 1976. In one case, it is narrower by 18 m (Figure 4).

Increases in channel depth were noted in all the examined reaches of the Raba River. Average increases equaled 1.8 m, with a maximum increase of 3.8 m in a downstream reach of the Raba river channel surrounded by levees (Figure 2). It is important to remember though that an increase in river channel depth in the Raba River is first and foremost caused by intense downcutting erosion occurring in the river following a period of intensive river regulation works.

Minimum annual water levels measured at gauging sites in the middle and lower course of the Raba River were used to assess the tendency towards channel deepening in the 20th century [10,52,53]. According to Wy ˙zga [10,53] the Raba river channel became deeper by 2 or 3 m in its downstream section in the 20th century. Nonetheless, both periods of increased erosion and gradual debris accumulation occurred throughout the 20th century in the Raba river channel (Figure 2). Łapuszek and Ratomski [52] provide similar results. In the years from 1901 to 1996 the downstream reach of the river became deeper by 3.79 m in Gdów and 1.76 m in Proszówka. In the upstream reach of the river, the onset of erosion dates to 1971, and by 2002 the river channeled had become, on average, about 1.4 m deeper (Figure 2).

Additional information on channel deepening in lower reaches comes from an analysis of damage to regulation structures in the Raba river channel. Damage data were collected for 26 river training structures built in the 1960s and 1970s, most of which were located in the upper sections of the Raba River (Figure 2). River training structures damaged by downcutting and lateral erosion serve as unique types of reference sites for the rate of erosional change. River channel deepening at such sites ranged from 0.45 m to 2.5 m. Intensive channel deepening at more than 2 m was also observed upstream of the backwater area of the Dobczyce Reservoir. This reach is currently experiencing significant accumulation. A very high rate of downcutting erosion could have been associated with the construction of the Dobczyce Reservoir.

Accelerated downcutting and lateral erosion in the Raba river channel led to undercuts in the riverbank. Today more than 75% of the Raba River reaches feature a larger area of undercuts in relation to 1976 (Figure 3). The present-day area of undercuts is three times larger than in 1976. The average area of undercuts per reach increased by 515 m2/km. Maximum increases in the area of undercuts per river reach equaled 3011 m2·km<sup>−</sup>1. An additional outcome of river regulation, although one not associated with downcutting erosion, is a rise in the length of sections of river dominated by water and sediment transport.

The most readily observable present-day change in the Raba river channel in comparison with 1976 is the increase in the area of bars (Table 1). Today the area of Raba bars is twice as large as that in the 1970s. Increases in bar and island areas, in 2015, relative to 1976 were noted in almost 75% of Raba River reaches and equal an average of 2190 m2·km<sup>−</sup>1. The largest increase in the area of accumulation landforms found in the Raba river channel reached almost 30,000 m2·km<sup>−</sup>1. It occurred at the point of confluence between the Raba River and one of its major tributaries, the Krzczonówka River (Figures 3 and 4). This reach was also characterized by the largest increase in river channel width. This reach has been viewed as a classic example of a bead of morphologic diversity strung on the string of the studied river channel [27]. Similar accumulation zones occur in most reaches of the mountain section of the Raba river channel. A total of six large accumulation zones and more than 25 rather small channel broadening zones with lateral bars were observed in the present study (Figure 4).

**Table 1.** Area of bars and undercuts in the Raba river channel.


The tendency described above is only seemingly inconsistent with the observed decline in the share of Raba river sections characterized by a predominance of deposition and redeposition processes. Deposition occurs along a shorter stretch of the Raba river channel, but it occurs with more intensity. In effect, reaches of channel where bar formation is a predominant morphodynamic process are characterized by channel widening. While the distribution of the area of bars along the Raba River remains uneven, it still differs from that in 1976, when, on the one hand, almost 50% of the area of bars

in the studied channel was to be found in a several-kilometer-long stretch on the boundary between mountains and a foreland basin. On the other hand, accelerated deposition of river channel material today occurs at a much larger number of reaches along the Raba River.

In 1976, the gravel fraction of bed material (diameter 2 to 64 mm) dominated in nearly all reaches of the Raba River. In 2015, the most evident change in the surface grain size distribution was an increase in the share of the pebble fraction of bed material (diameter 64 to 256 mm). Today, this is the dominant bed-material fraction in eight Raba river reaches, with most being located upstream of the Dobczyce Reservoir. An increase in the mean grain size of bed material was a general rule in regulated Carpathian rivers in the second half of the 20th century [5,54]. Raba river channelization in the period from the 1960s to the 1980s increased the transport ability of the river. The sediment supply by Raba river tributaries also diminished as they too were regulated resulting in little or no sand and silt being deposited in the river beds, with the material becoming coarser and better sorted, and channel bed armoring developing in some reaches of the river [55]. A surprising discovery was the decline in the maximum bed-material grain size in the Raba river channel between 1976 and 2015, which occurred in more than 50% of the studied reaches (Figure 3). The average decline was 3 cm. The largest decline in the maximum bed-material grain size (24.5 cm) occurred in one of initial reaches of the studied river. A large decline also occurred in several reaches below the Dobczyce Reservoir, i.e., an average of 12 cm. This is likely due to the retention of debris in the area upstream of the Dobczyce Reservoir. On the other hand, marked growth (more than 50 cm) in the maximum bed-material grain size between 1976 and 2015 occurred in two reaches of the Raba River downstream of the point of confluence with the Mszanka, which is the most important tributary of the Raba River in its mountain section.

The river's braiding ratio [33] also increased to some degree, by an average of 0.43 middle landforms per kilometer of river, over the 40 year period between the first and second survey. An increase in the braiding ratio was noted in more than 50% of the reaches in the study. The largest increase in the braiding ratio (4.4 middle landforms per kilometer) was noted in a reach of the Raba River found downstream of the Dobczyce Reservoir where a tributary flowed into the Raba River (Figure 3).

#### *5.2. Role of High Water Stages in the Evolution of a Post-Regulation River*

Floodwaters are an extremely effective channel-shaping factor. Large floods, in particular, are effective in floodplain development [25,56–61]. Their significance is examined in this section in terms of how they affect spontaneous renaturalization in a gravel-bed river during the post-regulation period, in this case, the Raba River. The morphological features and functioning of the river channel in 2009 and 2015 are compared for this very purpose.

The state of the Raba river channel in 2009 can be described by hydrodynamic conditions that would be the equivalent of a medium-high water. Such water-stages occurred following an earlier period with large floods from 1996 to 2001. However, the river channel experienced some changes during this earlier period due to the occurrence of major floods. It has adapted to more dynamic flow conditions following a period of low water levels since the early 1980s.

After 2009, the morphology of the Raba river channel was strongly affected by the most recent three large floods, two floods in 2010 and one flood in 2014. The flood in May of 2010 was characterized as a catastrophic flood based on the Punzet classification [62]. The flood occurred along the Raba River both upstream of the Dobczyce Reservoir and downstream of it. A second flood occurred in early June. While it was smaller than the May flood, it occurred at a hydrologically disadvantageous moment when water levels were still high in the river and groundwater levels were still high. The 2014 high-water stage was smaller than the first high-water stage in 2010, especially below the Dobczyce Reservoir (Q10%). However, in the upper reaches of the river it was higher than that in 2010. Water levels and discharge rates during the flood of 2014 were equivalent to a high-water stage that occurs once per 100 years (Q1%).

All the floods discussed above accelerated erosion and accumulation in the Raba river channel. The increase in the intensity of lateral erosion led to a widening of the river channel at about 50% of the studied reaches, although it did not affect the entire length of each reach. In areas where channel widening did occur, its width, in 2015, increased in most cases by several meters or several tens of meters relative to the year 2009. The river channel widened by more than 100 m relative to the year 2009 in several reaches, i.e., in the middle section of the river in the area where the Mszanka and Krzczonówka join the Raba River as well as in the section just below the Dobczyce Reservoir (Figure 4).

The area of bars also increased substantially throughout the Raba river channel after the floods of 2010 and 2014. By 2015 it was about 1.5 times larger than in 2009 (Table 1). The increase in the area of bars in the Raba channel, however, was not distributed evenly along the length of the river after the floods of 2010 and 2014.

In addition, increased channel sinuosity and the formation of multiple threads were observed in some reaches (Figure 4). The effects of the 2010 and 2014 flood events discussed herein are representative of the evolution of a river channel after a series of large floods, as described by the flood pulse model [21]. The widening of the channel and formation of a multithreaded river also suggest that connectivity between the river channel and floodplain has been regained for a period of time and the floodplain has reformed.

Today there are reaches of the Raba River that perform similar morphodynamic functions and repeat along the length of the river, although the morphodynamic functions of reaches also depend on the degree to which a river channel is regulated. Floods damage or destroy hydrotechnical structures, which is usually the first step in the shift from a channel's morphodynamic function, a transport function, or a downcutting function to a deposition function with lateral erosion.

The most dynamically evolving and morphologically diversified reaches of the Raba River were reaches that, already in 2009, were characterized by substantial sinuosity and large area of bars. These are mountain area reaches of the Raba River that were not "trapped" by road infrastructure and rural settlements.

The largest changes in the river channel were noted upstream of the Dobczyce Reservoir at sites where tributaries would supply large amounts of debris to the Raba River in the course of floods (Figure 4). Lateral erosion and deposition processes are very active at these sites, which has led to a rise in the Raba's riverbed due to the deposition of a portion of the material transported downstream of each point of confluence, as well as upstream of each point of confluence, due to limited discharge driven by abrupt increases in stream load in the confluence zone of the Raba and its tributaries. This evolution scenario for the Raba River was determined for reaches found downstream of the points of confluence of the following rivers: Olszówka, Kasiniczanka, Krzczonówka, and Bysinka (Figure 3).

Significant, although much smaller, changes in the morphology of the Raba river channel after foods were observed in the foothill section of the Raba channel downstream of the Dobczyce Reservoir. The retention of floodwaters and their sediment load by the Raba River inside the Dobczyce Reservoir limits the morphogenetic potential of flood events below the Dobczyce Dam. However, the floods of 2010 and 2014 have changed the morphodynamic function of these reaches from transport-dominated reaches to reaches with deposition with lateral erosion. A particularly large change in the morphology of the Raba river channel occurred downstream of the point of confluence of the Krzyworzeka River, which is also downstream of the Dobczyce Reservoir. In the flood period from 2010 to 2014 the channel of the Raba River made the transition from single-threaded to multi-threaded along this particular stretch of the river (Figure 4).

Straight and slightly sinuous reaches of the Raba River and reaches characterized by a small post-regulation width became only slightly altered during flood events in 2010 and 2014. As in the period prior to 2009, these reaches perform a mostly transport function, with small changes occurring in the channel due to the concentration of transported material along the main axis of the channel. These are reaches with mostly levees that are located in the lower course of the Raba, as well as two

reaches located within the city limits of two largest towns in the Raba Valley, Rabka and My´slenice (Figures 1 and 3).

The last large floods period was followed by a gradual process of adjustment of the river channel to "average" hydrodynamic conditions in line with the flood pulse concept [21]. This period of adjustment could become interrupted by major floods in the future.

### **6. Conceptual Model of the Evolution of a Gravel-Bed River during the Post-Regulation Period**

The fluvial system of a post-regulation river experiences a distorted debris supply pattern in its full longitudinal profile. A shortage of debris generates forces that aim to replenish the channel system with sediments. Erosion damages river training structures and liberates debris material into the channel system from the riverbanks and floodplain. A spatially uneven supply of debris from reaches experiencing less regulation pressure contributes to the formation of a number of wide accumulation zones similar to those discussed in the literature and designated sediment waves or sediment slugs [63,64]. The process of forming these zones is discontinuous. One additional characteristic of these zones in a post-regulation river is their limited mobility resulting from anthropogenic constraints in the river channel and the valley floor. A post-regulation river is characterized by long straight reaches and slightly sinuous reaches playing a primarily transport role where unit stream power values are high. Such reaches do not favor accumulation. Hence, the deposition of transported debris usually occurs in widened zones [65]. These zones can be classified as beads using the beads on a string conceptual model by Stanford and Ward [27].

The following four characteristic reach types were identified for post-regulation river channels based on the Raba River: (A) Regulated reaches, (B) reaches with destroyed regulation works but retained regulation channel, (C) sinuous reaches with bars, and (D) multithreaded reaches, i.e., deposition zones (Table 2 and Figure 5I,II). The first two types (A and B) are single-threaded, compact channels that often feature rock outcrops on the channel floor, characterized by low sinuosity and a W/D ratio implying a narrow, deep channel. The other two types (C and D) are channels at various stages of renaturalization. Type C is a single channel, sinuous, widened, and with bars. Type D is a multithreaded channel characterized by the highest W/D ratio, wide, with a number of threads and multiple mid-channel bars [8].


**Table 2.** Characteristics of the reaches of a post-regulation river.

Types A and B represent a narrow string, which is consistent with the idea of beads on a string. Both small beads (Type C) and large beads (Type D) are scattered along this string at irregular intervals (Figure 5). These four types of reaches alternate along the longitudinal profile of the studied river. However, some river reaches are more homogeneous, where one type will exist over a significant distance, whereas the channel structure in other reaches will be fragmented to a greater extent. Longer homogeneous reaches are found in Type A and B channels. Type C and D reaches occur irregularly along the course of the river and are separated by Type A and B channel reaches. This sort of spatially variable system of channel reaches is found in gravel-bed river valleys in the Carpathians and is accurately described by the beads on a string idea proposed by Stanford and Ward [27].

**Figure 5.** Conceptual model of the evolution of a gravel-bed river in a mountain area during a post-regulation period.

The location of the above-mentioned reaches, types A through D, in the river system is due to both natural determinants such as geologic structure, relief, and climate, as well as due to human impact associated with river channel regulation, road infrastructure, land use, and human settlement. This is why it is difficult to unequivocally determine the reasons for the occurrence of reaches of type C and D where the pattern of occurrence is the result of a combination of fluvial processes present in a post-regulation river (Figure 5I,II).

Spontaneous renaturalization occurs most intensively in reaches of type C and D, at locations where fluvial processes can proceed freely. Hence, spontaneous renaturalization along a post-regulation river does not occur in a continuous manner, but in a fragmented manner.

Type D reaches constitute initial sites of channel debris restoration in the river system. Debris accumulated in these zones comes primarily from bank erosion and is supplied by tributaries. These wide accumulation zones also serve as sites for the evolution of multithreaded systems and make it possible for the river channel to migrate freely (Figure 5II). The presence of type D reaches, and to a lesser degree type C reaches, is a sign of spontaneous renaturalization in a post-regulation river system. This process begins with the destruction of regulation structures and changes in principal fluvial processes along with a reduction in the share of downcutting and an increase in the share of lateral erosion, where type A and B reaches transition into type C reaches. In the next stage, type C reaches experience accumulation, expansion of the active zone, and expansion of the channel free migration zone or the formation of several channels. This process can occur gradually or abruptly in the course of a single large flood event where type C reaches transition into type D reaches. Type A and B reaches can also develop into type D reaches directly in the event of a catastrophic flood. However,

type A and B reaches can suffer further decline as a result of increased downcutting, which makes it impossible for them to transition into type C. In the event of repeated river regulation, type B, C, and D reaches can transition back to type A (Figure 5II).

These wide alluvial reaches (type D) represent a source of channel material, and their evolution follows three different directions as follows: (1) They can become wider, (2) they can become longer, and (3) they can become thicker. The expansion of this zone in a post-regulation river is associated with lateral erosion. This is a necessary precondition for the river renaturalization, as the river is "trapped" in a deep-cut channel and a narrow, regulated flow pathway. Lateral erosion and accumulation are linked processes in this case. Extension of the accumulation reach or its migration along the length of the river is often made difficult by various forms of human impact in the valley. Difficulties include road infrastructure, close proximity to buildings, and river training structures.

The thickness of debris layers increases, as does the width and length of sedimentation zones in the course of flood events. These are zones wherein the river channel can freely migrate and consist of one or more threads and wide bars not covered with perennial vegetation. A period of several years without floods leads to changes in the functioning of the widened channel migration zone, where a river can freely choose its flow pathway (Figure 4III).

In periods without major floods, fluvial processes usually become limited to a narrower zone, i.e., the encroachment of vegetation onto bars, the decline of discharge inside the channels, and the limiting of discharge into the most deeply incised channel narrows down the active zone of the free migration zone. What remains in the active zone is a channel with a low level of water and bars not covered with vegetation [66,67]. However, this remains a zone for accumulation, and it is readily available to fluvial processes during subsequent floods. While this depends on the magnitude of the next flood, this zone can become only refreshed or it can become expanded.

This expansion can occur via the undercutting of floodplain terraces, which incorporates more land into the migration zone. In a post-regulation river, this process is limited in scope. A river that is "trapped" between road embankments, various other structures, or levees has only so much leeway to migrate. This pulse-type pattern of the evolution of accumulation zones with the capability for free migration during flood events and a narrowed down active zone between floods can be conceptually associated with the idea of a flood pulse [21,22] in a geomorphologic sense.

The final research question concerns the direction that mountain river systems are headed during the post-regulation period having been subjected to significant human impact in the last 100 years. Is it possible for river systems to return to their functioning from the 19th century? Or, will completely new channel patterns emerge as a way of adjusting to contemporary factors? A complete answer to these questions is not possible as of today. Currently river systems during the post-regulation period are in their initial stage of spontaneous renaturalization. In order to produce forecasts, it is necessary to conduct more research in such systems over the next few decades or at least over the next decade or so.

### **7. Conclusions**

Compared with the 19th century, present-day river channels in the Carpathians possess more transport capacity, receive a smaller supply of catchment debris due to changes in land use, have a narrower free migration zone, experience less lateral erosion due to reinforced banks, and follow a distorted (i.e., narrowed and straightened) flow path that is not adapted to natural conditions.

Major changes in the morphology of post-regulation river channels occur mostly in the course of flood events. The initial stage of spontaneous renaturalization includes at least two potential channel evolution scenarios. A river channel can evolve in the direction of an accumulation channel with lateral erosion. In the second scenario, a river channel experiences erosion that helps make permanent its regulated structure. Both scenarios can play out in the same river channel, but in adjacent reaches. This indicates great complexity and fragmentation of the structure of a post-regulation river channel. In initial spontaneous renaturalization stages, this process can occur in limited sections and does not

need to affect the entire channel system. In the case of river channels situated in urbanized areas, this process could never materialize. The same is true of fully regulated river reaches.

New patterns of channel evolution observed in river channels now affected by spontaneous renaturalization could be indicative of how gravel-bed rivers in mountains areas will evolve in the 21st century if human impact is reduced.

**Author Contributions:** Conceptualization, E.G. and K.K.; data curation, E.G.; investigation, E.G. and K.K.; methodology, E.G. and K.K.; software, E.G. and K.J.; visualization, E.G.; writing—original draft, E.G., K.J. and K.K.; writing—review and editing, K.J. All authors have read and agreed to the published version of the manuscript.

**Funding:** This research received no external funding.

**Conflicts of Interest:** The authors declare no conflict of interest.
