Wednesday, July 20, 2016

OMS Summer School 2016 - What we actually did

This is what we actually did at the Summer School on OMS3. Here you will find slides and material (actually, it is already presented in the Colorado State University site), but I will document here a little more. (Still a work in progress)


Wuletawu Abera (University of Trento, Italy)
Olaf David (Colorado State University, Fort Collins, US)
Giuseppe Formetta (Centre for Ecology and Hydrology, Wallingford, UK)
Tim Green (Agricultural Research Service, Fort Collins, US)
Greg McMaster (Agricultural Research Service, Fort Collins, US)
Scott Peckham (University of Colorado, Boulder, US)
Riccardo Rigon (University of Trento, Italy)
Francesco Serafin (University of Trento, Italy)
Marialaura Bancheri (University of Trento, Italy) 

Monday -  Introduction, Component-based Modeling Concepts 

09:00 - 12:30 Scope of the class
  • Class introduction (Rigon) - I could not be present, so someone talk in my place. 
          I think what I would have to tell you is here.
          Other information on Naming things in hydrology is here. However, Scott's presentation in                 presentation 2 is pretty informative.
14:00 - 17:30 Getting Started with OMS(David)

Tuesday -  OMS Introduction

09:00 - 12:30 
  • Component Integration (David)  Presentation 
  • The Water tank example (Peckham, David) 

      The water tank  example is very simple, but very illustrative of what a model is. Today there is a         tendency to think lumped models as a set of tanks with rules for moving water. I will do a post             soon for it.

14:00 - 17:30 OMS Basic Building Blocks (cont.) Step By Step 
  • Project structure, components, simulations, file formats, annotations, etc. ( )
  • Simulation Development. (scripting, testing, component connectivity, Examples
  • Thornwaite Waterbalance Model example
References: Annotations, DSL, CSV, OMSConsole

Wednesday Modeling Applications I

09:00 - 12:30 Hydrological modelling JGrass-NewAGE (Abera)

14:00 - 17:30 Model calibration algorithms in NewAge-JGrass(Formetta)


References on JGrass-NewAGE can be found here. References on the Horton Machine can be found here. Maybe for most of you is a mystery what Pfafstetter numbering is. You can find information here. If someone has further doubts on components, they are documented on the GEOFRAME blog. If you do not have experience with calibration algorithms, you could start from some recent paper by Hoshin Gupta.

Addedum. Giuseppe added also a presentation of what he did on simulating landslides triggering with GEOtop (by embedding it in OMS3).

Thursday Modeling Applications II 

09:00 - 12:30 Agricultural Ecosystem Services (AgES) Watershed Model (Green)
  • Model Description  
  • How to run AgES in the OMS Console (Quick Start)
  • Brazil case study (streamflow)
  • Colorado, USA case study (distributed soil moisture)
AGEs is a "storages" based model, meaning that, as many other modern models, is based on the concept of intercommunicating storages. Physical contents are highly parameterised, but the model works. One of the model characteristic, which is common to other agricultural-oriented hydrological models, is the subdivision in small parcels with multiple communications among them (called Hydrologic Response Units). Interesting also the slides regarding the complexity of models.

14:00 - 17:30 Plant growth modeling with AgES (McMaster)

Monday, July 11, 2016

The first taste of Ne3 (netree) (at IEMSs in Toulouse)

We had this presentation, this morning at IEMSs, about some of the many lines of work where Francesco Serafin (his blog here) is developing his Ph.D research. The origin of the work is that modelling basins is to model hillslopes (or Hydrologic Response Units, HRUs) connected by a river network. Most of what happens in HRUs is independent from what happens in the others. Some instead is aggregated by river network. So why do not use this natural structure to organise modelling and processes (and send them in parallel, when possible, using the tree structure) ?
Actually this can grow more, since many systems (a plant, ecological interactions, hydrological interactions), can be seen described over a graph of interactions. So the Ne3 can become a more general way to investigate natural systems. However, you can enjoy the presentation, by clicking on the figure above.  Ne3 source code written so far in on Github.

Sunday, July 10, 2016

JGrass-NewAGE at IEMSs in Toulouse 2016

JGrass-NewAGE is growing and the readers of this blog know it. We are presenting the state-of-art-of the infrastructure in Tolouse IEMSs biennial meeting, and the presentation that will be given by Marialaura Bancheri is below (click on the Figure).
Improvements are not only on the number of components, but also in their internals. Many components now runs faster and are less error-prone. At the end of the presentation you can find the links to relevant papers. Enjoy!

Monday, July 4, 2016

Climaware Trailer

Do people know what us scientists do ? In trying to make the people aware of our project, we produced (Nadja Grasselli director, together with Daria Akimenko) this trailer about our project CLIMAWARE.
CLIMAWARE - Trailer from LMN - Liminale Räume on Vimeo.

The full video where we try to explain who we are and what we do is here.

Thursday, June 30, 2016

Celerity versus velocity and the travel time problem

A little of introduction

Velocity of a fluid is the variation of its particles' position with time. Celerity is the speed at which a signal (a wave) is transmitted trough a medium. Velocity of particles determines flows (fluxes) out of a control volume. Celerity, as we will see, modify the particles' velocity field (intensity and extension).

Jeff McDonnell (GS), and Keith Beven (GS) (J&K) with their nose for interesting topics, recently wrote  a paper where they discuss the role of the two quantities with reference to travel time problems. Some other papers (e.g. Kirchner, 2016,  Hrachoitz et al, 2013) echo the same problem. 
One important point that Beven and McDonnell discuss is that transport of properties (passive tracers) depends on water molecules velocity and therefore between transported properties (like temperature, water isotopes, water age) and flow (assumed to be dominated by celerities) can be various discrepancies.

Travel time, $T_r := t-\tau$ is described in literature by its probability $p(t-\tau|t) $, where $t$ is the actual time,  $\tau <  t$ is the injection time and $p(t-\tau|t)$ is the travel time distribution conditional to the actual time.  For details about travel time distribution, residence time and life expectancy of water particles, please take the time to read this discussion paper. Implicitly, it is assumed that the probability is evaluated at the closure (boundary) of a control volume.  The distribution represents the ensable distribution of infinite random experiment that regards the motion of a single molecule or, after the hypothesis of ergodicity, the distribution of the travel time of a bunch of molecules, which are injected together in the system, in different positions.

Actually J&K argued about the mean travel time $<T_r >_t$ more than of its distribution. $<T_r >_t$ definition is:

$<T_r >_t := \int_0^\infty (t-\tau) p(t-\tau|t) d(t-\tau) $

J&K (and the other papers) said that $<T_r >_t$  is affected both by velocity and celerity but I do not think they went right to point. One central fact is that, as follow from Botter et al., 2010, 2011, discharge is estimated through a different probability distribution function, which is $p(t-\tau|\tau)$:

$ Q(t) = \int_0^t p(t-\tau|\tau) J(\tau) d\tau $

where $Q(t)$ is the total outflow from a control volume and $J(\tau)$ is the precipitation input. Therefore the breakthrough curve (the backward probability) and the fluxes are not, usually,  linearly related.
$p(t-\tau|\tau)$ and $p(t-\tau|t)$ are not completely independent and are related by the Niemi's relationship

Back to the basics

Let’s me re-discuss the topic from the scratch. When we have a velocity field, $u(\vec{x},t)$ in a fluid it can be either stationary or time varying. Assume it is stationary. Then:

$\frac{\partial u(\vec{x},t)}{\partial t} = 0$

which implies that $u(\vec{x},t) = u(\vec{x})$, i.e. the velocity field, does not depend on time, and it is called stationary. Does it imply that forces do not act ? No. Forces act, because still we can have gradient of velocity:

$\nabla u(\vec{x}) \equiv (\frac{\partial u(\vec{x})}{\partial x}, \frac{\partial u(\vec{x})}{\partial y}, \frac{\partial u(\vec{x})}{\partial z} ) \neq 0 $

So, when the we follow a particle moving (the so called Lagrangian view of fluid motion), it is locally accelerated, and it feels a force. However, forces do not change in time and are subject to stationary resistances (dissipation) that do not allow for the overall system to accelerate (increase the total kinetic energy). 
If a second particle is injected in the same place of the first one, it will have the same travel time. Particles (parcels, molecules) injected in different points will have different trajectories, all stationary, and the overall distribution of of travel times for a bunch of particles injected together (or, BTW, at a different time) is not time varying. It has to be remarked that the fluxes that come out from such a velocity field is not constant but reflect the mass (volume) of particle injected in the fields. Furthermore, we can say what is going in, will go out in a certain composition of ages which  is relatively easy to disentangle from the knowledge of the spatial field and the amount of injected matter.  
In the above case no net energy is transferred and we do not have to invoke celerity but just velocity. 

Now, assume we have a time varying velocity field, so that $u=u(\vec{x},t)$ and:

$ \frac{\partial u(\vec{x},t)}{\partial t} \neq 0$

This implies we have acceleration in (usually) many points which must be generated by a local force (which has to be time varying). The way to obtain it in a fluid is to generate a time-varying pressure gradient (yes, excluding time varying gravity, time varying electromagnetic fields, time varying applied work, time varying temperature or density gradient etc. , all things we usually not deal with in our hydrological problems). Actually it can be shown that these pressure variations, once imposed, can travel from one place to another (in ways that are different in different phenomena: see J&K for the enumeration of some cases) so that this pressure variation is the cause of the varying velocity field. The speed of these travelling pressures is the celerity we (and J&K and others) are talking about. Conjointly with velocity field variations, fluxes in previously unaffected portionof the control volume can be activated.
Therefore the distribution of particles’ travel times is affected in two ways: by mobilising water (and/or enlarging the sectional area) and by increasing (locally) water velocities.
From the above analysis is also evident that the phrase "celerity (of pressure waves) affects flows" is true, but in an indirect way, since flow is affected by velocity field and its spatial extension (no less, no more), but both are modified by pressure waves. Moreover, if we exclude surface water where these pressure variations are visualised by up-and-down of the free surface (the waves), using "celerity of water" is meaningless, and, for the generic case, an imprecise naming.

Consequences on the mean travel time

In the case of time varying velocity fields, distribution of the mean travel time can vary because the new activated area can contain water of ages different from those activated previously, and because locally the velocity of water can increase (or decrease) at the passage of the pressure wave.
The latter effect can skew the distribution of travel time to the left (to smaller or larger travel times), but unless the variation is such that the whole the control section is affected (which can be the case), it has not significant effects on the mean travel time, which is an integrated quantity.
Due to time variation of the velocity field, when we inject two water volumes in the same place at different times, the travel time of the two volumes is different, and consequently, the related transported quantities. The travel time distribution $p(t-\tau|t)$ is therefore time-variant, and we can attribute this variation to the effect of celerity, meaning that there are pressure waves propagating in the control volumes. However the expression for the mean travel time is always the same.

Well, the velocity field is not superimposed, but caused by the quantity of water itself.

So far we discussed the cause of  varying velocity fields which I suggested was due to pressure waves. These, in case of water flow are usually generated by variations of the water amount itself. The velocity field, in fact, is not something independent of the water quantity and distribution and, on the contrary, depends on it. So when we inject water, we cause pressure waves that propagates with a law dependent on the medium: at the surface, in the vadose zone, or in the ground. (Therefore the idea of a stationary flow field with varying water inputs is not, in general, a credible assumption. It can be an approximation to take with care).

I think there is no mystery in all of it.

Post Scriptum (July 8/2016)

I realised that what I wrote was overlooking the normal view (and problems) researchers in the field have about travel time distribution.  The reference is the beautiful (a must read) work Dagan, 1984 cited below. Dagan and followers observe that there is diffusion and, moreover, stationary velocity field can be very heterogeneous.  I forgot diffusion, and, whilst accounting for the second, I did not stressed enough the consequences of heterogeneity on travel time distributions.  For this, the reading of Dagan's paper can be enough.  What I said, however, remains true.


Botter G, Bertuzzo E, Rinaldo A, 2010. Transport in the hydrologic response: Travel time distributions, soil moisture dynamics, and the old water paradox. Water Resources Research 46(3): n/a–n/a. ISSN 1944-7973. doi:10.1029/2009WR008371.

Botter G, Bertuzzo E, Rinaldo A, 2011. Catchment residence and travel time distributions: The master equation. Geophysical Research Letters 38(11): L11403. ISSN 1944-8007. doi:10.1029/2011GL047666.

Dagan, G. (1984). Solute transport in heterogeneous porous formations. Journal of Fluid Mechanics, 145, 151–177.

Hrachowitz, M., Savenije, H., Boogard, T. A., Tetzlaff, D., & Soulsby, C. (2013). What can flux tracking teach us about water age distribution patterns and their temporal dynamics?, Hydrol. Earth Syst. Sciences, 17, 533–564.

Kirchner, J. W. (2016). Aggregation in environmental systems – Part 1: Seasonal tracer cycles quantify young water fractions, but not mean transit times, in spatially heterogeneous catchments,  Hydrol. Earth Syst. Sciences, 279–297.

McDonnell, J. J., & Beven, K. J. (2014). The future of hydrological sciences: A (common) path forward? A call to action aimed at understanding velocities, celerities and residence time distributions of the headwater hydrograph. Water Resources Research, 50, 5342–5350.

Niemi AJ, 1977. Residence time distributions of variable flow processes. The International Journal of Applied Radiation and Isotopes 28(10–11): 855 – 860. ISSN 0020-708X. doi:

Tuesday, June 21, 2016

Is possible to get the runoff for European Countries ?

This is a conversation between two groups of the CLIMAWARE project of some general interest. Further information about global or continental scale hydrology can be found in some previous posts.

Dear Alberto and Riccardo

we are writing about the data we need for the project CLIMAWARE. 

The objective of out analysis is to estimate the impacts on agricolture of modification of:

1)  soil use
2)  anything due to the changed water availability as a consequence of the climate change. 

We are thinking to consider two time frames, the first up to 2020, the second up to 2040 (this because the estimation of soil use variation are available for these two dates and to do an analysis on the national scale for all the Countries of the European Community. 

Alberto's answer:

Dear Martina,

for what I know, there are not detailed projections at this scale. I saw studies on the largest basins (as  Danube) where all is solved by putting R = P- E (runoff = precipitation - potential evapotranspiration). For what I know, nobody looks at the national scale, for the reasons that the river basins do not coincide with nations areas.

There are regional studies (not about the countries but  for Southern Europe, for instance) made by Giorgi’s group or by Julich’s colleagues using their Earth system model. 

Bruno Majone answer:

Dear Martina,
what you are opening is a Pandora’s vessel. I try to explain it better. To deal with water availability at European scale, there are many different approaches. The simplest is to do a hydrological budget simply by using the available climatic projections. Alternatively, one can use hydrological models working at pan-european scale that can be fed directly by the projections themselves. For any of the choices the real problem is selecting the right forcings. There isn’t a reference dataset: there are various “ensemble” of simulations derived from various climate models, each one of them following a different pathways scenarios.  The reference initiative for Europe is Euro-cordex that gathers the modelling work of various research groups that perform experiments with global and regional climate models, and scale down the results from a coarse grid of 125 km to one of around 25 km (see the pdf). Considering the results of these models one should observe that usually they have strong biases that need to be corrected. Otherwise the water budgets can be extremely wrong. For what I know, inside the Euro-Cordex group there are groups that are examining and providing scenarios by using various techniques of bias correction, but I am not sure that they are already available and usable. 

If your interest is to have annually aggregated data by country, I personally would not explore thid road because I believe that the effort to contact the active groups, download huge datasets and precess them could be overwhelming.

I would try instead to contact groups that already have hydrological models setup at European scale and are already estimating climate change impacts. Alberto mentioned the Julich group, but another possibility could be JRC. They have their model LIFSFLOOD set up at 5*5 km of resolution (and it could be that they already have used it to do some impact studies).  At this point you should ask for they to send some gridded data of runoff and afterwards aggregate them at country level.