Issue 
A&A
Volume 602, June 2017



Article Number  A21  
Number of page(s)  19  
Section  Planets and planetary systems  
DOI  https://doi.org/10.1051/00046361/201630013  
Published online  24 May 2017 
Planetesimal formation near the snowline: in or out?
Anton Pannekoek Institute for Astronomy, University of Amsterdam, Science Park 904, 1090 GE, Amsterdam, The Netherlands
email: d.schoonenberg@uva.nl;
c.w.ormel@uva.nl
Received: 4 November 2016
Accepted: 4 February 2017
Context. The formation of planetesimals in protoplanetary disks is not wellunderstood. Streaming instability is a promising mechanism to directly form planetesimals from pebblesized particles, provided a high enough solidstogas ratio. However, local enhancements of the solidstogas ratio are difficult to realize in a smooth disk, which motivates the consideration of special disk locations such as the snowline – the radial distance from the star beyond which water can condense into solid ice.
Aims. In this article we investigate the viability of planetesimal formation by streaming instability near the snowline due to water diffusion and condensation. We aim to identify under what disk conditions streaming instability can be triggered near the snowline.
Methods. To this end, we adopt a viscous disk model, and numerically solve the transport equations for vapor and solids on a cylindrical, 1D grid. We take into account radial drift of solids, gas accretion on to the central star, and turbulent diffusion. We study the importance of the backreaction of solids on the gas and of the radial variation of the mean molecular weight of the gas. Different designs for the structure of pebbles are investigated, varying in the number and size of silicate grains. We also introduce a semianalytical model that we employ to obtain results for different disk model parameters.
Results. We find that water diffusion and condensation can locally enhance the ice surface density by a factor 3–5 outside the snowline. Assuming that icy pebbles contain many micronsized silicate grains that are released during evaporation, the enhancement is increased by another factor ~2. In this “manyseeds” model, the solidstogas ratio interior to the snowline is enhanced as well, but not as much as just outside the snowline. In the context of a viscous disk, the diffusioncondensation mechanism is most effective for high values of the turbulence parameter α (10^{3}–10^{2}). Therefore, assuming young disks are more vigorously turbulent than older disks, planetesimals near the snowline can form in an early stage of the disk. In highly turbulent disks, tens of Earth masses can be stored in an annulus outside the snowline, which can be identified with recent ALMA observations.
Key words: accretion, accretion disks / turbulence / methods: numerical / planets and satellites: formation / protoplanetary disks
© ESO, 2017
1. Introduction
Planets form in gaseous disks around young stars. Initially, micronsized dust grains are present in such a disk. It is generally thought that planets form from planetesimals of the order of a kilometer in size, which are large enough for gravity to play an important role (Safronov 1969; Pollack et al. 1996; Benz 2000). However, the first step in the planet formation process, the coagulation of dust grains into planetesimals, is still an unsolved problem. Although micronsized grains can quite easily coagulate to mmsized particles (Dominik & Tielens 1997; Ormel et al. 2007), typical relative velocities quickly become so large that particles fragment or bounce rather than stick (Blum & Wurm 2000; Zsom et al. 2010). The typical size at which coagulation is no longer feasible is referred to as the fragmentation or bouncing barrier. Observations at radio wavelengths indeed infer a large reservoir of these mmtocm size particles (pebbles) (e.g., Testi et al. 2014).
Even if it were possible to coagulate uninterruptedly from micronsizes to large bodies, the growth process would face another challenge: that of radial drift. As soon as particles reach sizes at which they aerodynamically start to decouple from the gas, they lose angular momentum and spiral towards the star (Whipple 1972; Weidenschilling 1977). Radial drift is a fast process and hence poses a challenge to planetesimal formation theories, as planetesimals should form before the solids are lost to the star.
A promising mechanism to quickly form planetesimals directly from pebbles is streaming instability (Youdin & Goodman 2005; Johansen et al. 2007; Johansen & Youdin 2007). Streaming instability leads to clumping of pebbles that subsequently become gravitationally unstable and form planetesimals. In order for streaming instabilities to occur, the metallicity of the disk has to be locally enhanced above the typical value of 1% (Johansen et al. 2009; Bai & Stone 2010; Dra¸żkowska & Dullemond 2014). However, if one considers a smooth disk (i.e., without any radial pressure bumps or special locations), solids are flushed to the star in an insideout manner due to dust growth and radial drift (e.g., Birnstiel et al. 2010, 2012; Krijt et al. 2016b; Sato et al. 2016)^{1}. Radial drift lowers the metallicity of the disk and – at first sight – works against creating conditions favorable to streaming instability.
A special location that can affect the distribution of solids in the disk is the snowline. The snowline is the radius from the central star interior to which all water is in the form of vapor. Recent observations of structures in protoplanetary disks (for example HL Tau; ALMA Partnership et al. 2015) have been proposed to be associated with icelines (not necessarily water), e.g., Banzatti et al. (2015), Okuzumi et al. (2016), Nomura et al. (2016).
The viability of a pileup of solids at the snowline has been a topic of interest for considerable time. Several mechanisms have been proposed, such as the creation of a pressure maximum (e.g., Brauer et al. 2008) or a deadzone (e.g., Kretke & Lin 2007). Another pileup mechanism is water diffusion and condensation: water vapor in the inner disk can diffuse outward across the snowline and condense, thereby increasing the solids reservoir just outside the snowline. Works that have investigated the role of water diffusion and condensation on the growth and distribution of solids include Stevenson & Lunine (1988), Cuzzi & Zahnle (2004), Ciesla & Cuzzi (2006), Ros & Johansen (2013), Estrada et al. (2016), Armitage et al. (2016) and, recently, Krijt et al. (2016a), which focuses on the atmospheric snowline. In this paper, we investigate the role of the radial snowline to enhance the solidstogas ratio.
The works most relevant to our problem are Stevenson & Lunine (1988) and Ros & Johansen (2013). Stevenson & Lunine (1988) investigated the role of outward diffusion of water vapor across the snowline. In their work, a “coldfinger” effect was considered: water vapor from the inner disk condenses on (preexisting) solids beyond the snowline. In this way, they found a steep increase in the solid density beyond the snowline and hypothesized that this could accelerate the formation of Jupiter. However, dynamical aspects of the disk, such as radial drift of solids and accretion of gas, were not taken into account; except for the vapor, their model is essentially static. More recently, Ros & Johansen (2013) also simulated pebble growth by condensation, adopting a Monte Carlo method. In their simulation, the purely icy particles grow by condensation, until the point that they are “lost” by evaporation (modeled as an instantaneous process). Because their work does not feature silicate “seeds” that are immune to evaporation, the remaining ice particles can only grow in size. Consequently, a steadystate is never reached, also not because the simulation domain does not connect to the rest of the disk: there is no inflow of small pebbles or removal of vaporrich gas.
In this work we consider a model that emphasizes the dynamic nature of the disk, characterized by the accretion rates of pebbles and gas. Our model of the iceline therefore includes inflow of pebbles (at the outer boundary) and outflow of vapor (at the inner boundary) – a design that results in a steadystate. Our goal is to investigate whetherornot this more dynamic design will result in a solids enhancement that could trigger streaming instabilities. In particular, we will investigate how the solidstogas ratio will depend on the properties of the disk: the accretion rates (of solids and gas), the turbulence strength, and the aerodynamical properties of the drifting pebbles. We will also investigate which side of the snowline the solidstogas ratio is boosted most: interior or exterior.
We use a characteristic particle method, assuming a single pebble size at each time and location in the disk (Ormel 2014; Sato et al. 2016). We numerically solve the partial differential equations that govern the transport and condensation/evaporation processes for solids and vapor. We consider two model designs for the composition of pebbles: “single seed” (all silicates in one core) and “many seeds” (many tiny silicates grains). Our model also accounts for feedback of solids on the gas (a.k.a. collective effects) and feedback of water vapor on the scale height of the disk. A semianalytic model is presented that approximates the numerical results, enabling us to carry out parameter searches.
We start out with a description of our model in Sect. 2. In Sect. 4 we discuss numerical results for a fiducial set of model parameters in detail. We first describe the timedependent numerical results in Sect. 4.1, after which we focus on the steadystate solution in Sect. 4.2. In Sect. 5 we summarize the semianalytical approximate model (which is described in more detail in Appendix C) and present our results concerning streaming instability conditions. We discuss our results in Sect. 6 and present our main conclusions in Sect. 7. A list of frequently used symbols can be found in Table A.1.
2. Model
2.1. Disk model
Throughout this paper, we use the αaccretion model (Shakura & Sunyaev 1973) to model disks. We fix the mass of the central star M_{⋆} = M_{⊙}. We fix the temperature profile T(r) to: (1)where r is the radial distance from the star. This temperature powerlaw profile corresponds to a passivelyirradiated disk and a solarmass star (Kenyon & Hartmann 1987; Armitage et al. 2016); for simplicity, we neglect viscous heating. The isothermal sound speed c_{s} is related to the temperature as: (2)with k_{B} the Boltzmann constant and μ the molecular weight of the gas, which is 2.34 times the proton mass for a typical solar metallicity gas. The disk scale height H_{gas} is given by: (3)where Ω is the Keplerian orbital frequency. The gas accretes to the central star at a rate Ṁ_{gas}. Given α and Ṁ_{gas}, the steadystate gas surface density is (LyndenBell & Pringle 1974): (4)where v_{gas} = 3ν/ 2r is the radial speed of the accreted gas, with ν the turbulent viscosity, which is given by: (5)where α is the dimensionless turbulence parameter. As a result of our choices for the temperature and scale height profiles, Σ_{gas}(r) is a powerlaw with index − 1. We take the turbulent gas diffusivity D_{gas} equal to the turbulent viscosity ν.
2.2. Radial motion of ice, silicates and vapor
In this study, we are interested in the pebblesized fraction of the solids – we do not consider the smallersized dust. Pebbles are characterized by the fact that they are aerodynamically partly decoupled from the gas disk. The gas disk is partly pressuresupported, and therefore rotates at a subKeplerian velocity. The pebbles do not feel the pressure gradient, and therefore tend to move toward Keplerian orbital velocities. This means that pebbles are moving through a more slowly rotating gas disk, thereby losing angular momentum through gas drag. The loss of angular momentum results in pebbles spiralling (“drifting”) towards the central star. The extent to which pebbles drift depends on the stopping time t_{stop}, which measures how strongly the pebbles are coupled to the gas – it is the time after which any initial momentum is lost due to gas friction.
Concerning the stopping times of pebbles we can distinguish between two regimes: in the Stokes regime, the particle size is larger than the meanfree path of the gas molecules l_{mfp}, and the stopping time is calculated in a fluid description; in the Epstein regime, the particle size is smaller than the meanfree path of the gas molecules, and a particle description is needed instead. The meanfree path l_{mfp} is given by: (6)where σ_{mol} is the molecular collision crosssection, and ρ_{gas} is the gas density. We take σ_{mol} = 2 × 10^{15}cm^{2} as the collisional crosssection of molecular hydrogen (Chapman & Cowling 1970). The stopping time is given by: (7)where s_{p} is the particle radius, ρ_{•,p} is the particle internal density, and v_{th} is the thermal velocity of the gas molecules, defined as . The dimensionless stopping time (sometimes referred to as the Stokes number) is τ_{S} = t_{stop}Ω.
The radial drift velocity of pebbles v_{peb} is given by (Weidenschilling 1977; Nakagawa et al. 1986): (8)where ηv_{K} is the magnitude of the azimuthal motion of the gas disk below the Keplerian velocity v_{K}: (9)with P the gas pressure. Under normal disk conditions, the solidstogas ratio is about 1 in 100, and it is reasonable to neglect the backreaction of the solids on the gas. In this paper we are interested in situations where the solidstogas ratio is boosted, however, and therefore we study the effects of the backreaction of solids on the gas, or “collective effects”, as well. Collective effects have been calculated by Nakagawa et al. (1986). However, their formula was derived in the inviscid limit. In Appendix B we have calculated the drift velocity, accounting for both the backreaction and viscous forces. When including the backreaction, we replace Eq. (8) by Eq. (B.7).
Water vapor (denoted by the subscript Z) mixes with the gas and gets accreted to the central star at the same velocity as the gas.
2.3. Evaporation and condensation
The rate of change in mass (dm_{p}/ dt) of a spherical icy pebble is given by (Lichtenegger & Komle 1991; Ciesla & Cuzzi 2006; Ros & Johansen 2013): (10)where s_{p} is the radius of the pebble, v_{th,Z} is the thermal velocity of vapor particles, ρ_{Z} is the vapor density, P_{Z} is the vapor pressure, and P_{eq} is the saturated or equilibrium pressure, which is given by the ClausiusClapeyron equation: (11)where T_{a} and P_{eq,0} are constants depending on the species. For water, T_{a} = 6062 K and P_{eq,0} = 1.14 × 10^{13}gcm^{1}s^{2} (Lichtenegger & Komle 1991).
Assuming spherical pebbles and one typical particle mass m_{p} at each location and time in the disk (i.e., the particle size distribution is narrow), and using the ideal gas law to write P_{Z} in terms of the (midplane) vapor density ρ_{Z}, we can rewrite Eq. (10) into a change in the ice surface density Σ_{ice} due to condensation and evaporation: (12)where the dot denotes the time derivative. In Eq. (12) the vapor surface density Σ_{Z} is related to the midplane vapor density as and R_{c} and R_{e} are the condensation rate and evaporation rate, respectively, defined as: with k_{B} the Boltzmann constant, and μ_{Z} = 18m_{H} the mean molecular weight of water vapor, where m_{H} is the proton mass. Evaporating ice turns into vapor, and condensing vapor turns into ice, and therefore we find for the vapor source terms: (15)
2.4. Internal structure and composition of pebbles
We assume that in the outer disk, half of the mass in pebbles consists of water ice, and the other half consists of silicates (Lodders 2003; Morbidelli et al. 2015). That is, the dustfraction in pebbles in the outer disk ζ = 0.5. Adopting ρ_{•,ice} = 1gcm^{3} as the density of a pure ice particle and ρ_{•,sil} = 3gcm^{3} as the density of a pure silicate particle, we find that in the outer disk, the internal density of a pebble is ρ_{•,p} = 1.5gcm^{3}. Generally, the internal density of an ice/silicate pebble is given by: (16)where m_{ice} is the mass in ice within the pebble and m_{sil} is the mass in silicate within the pebble. Equation (10) is valid for a pure ice particle, while we use it for icy pebbles with (a) silicate core(s). We checked that using m_{ice} instead of m_{p} in the condensation and evaporation rates does not change the results significantly.
We consider two possibilities for the internal structure of icy pebbles (Fig. 1).

Singleseed model. In this model we view pebbles in the outer diskas balls of ice with a single core made of silicates. When the ice insuch a pebble evaporates, the silicate core is left behind. In thisframework, the number of pebbles does not change whencrossing the snowline.

Manyseeds model. In this model we view icy pebbles as lots of small silicate particles that are “glued” together by ice. The small silicate particles are released by evaporation, and free silicates can stick onto icy pebbles. We do not “resolve” the internal structure of the pebbles, and only trace the total amount of silicates “locked” into icy pebbles. Following Saito & Sirono (2011), we assume that the released silicate particles are of micron size. Because they are so small, the silicates do not undergo any aerodynamic drift and follow the radial motion of the gas.
Fig. 1
Schematic showing the difference between the singleseed model and the manyseeds model for the internal structure of icy pebbles in the outer disk. In the singleseed model, the water ice layer (white) on the silicate core (red) becomes smaller at the evaporation front, and after complete evaporation of the ice, only one single silicate core remains. Since we take ζ = 0.5, the silicate core contains half the mass of the original pebble: m_{core} = m_{ice} = 0.5m_{p,start}. In the manyseeds model, pebbles in the outer disk consist of many micronsized silicate grains (red) “glued” together by water ice (white). As the ice evaporates, silicate grains are released as well. After complete evaporation of the ice, many micronsized silicate grains remain. Again, with ζ = 0.5, the total mass in silicate grains in a pebble in the outer disk is half of the total pebble mass, but this mass is now divided among many silicate grains that each have mass m_{sil}. See text for more details. 
2.5. Transport equations
In this subsection we provide the systems of transport equations corresponding to both pebble composition models presented in Sect. 2.4. Our model is 1D; we integrate over the vertical dimension of the disk and follow column (surface) densities. Midplane densities are calculated assuming a Gaussian distribution in height with scaleheights H_{gas} (for the gas and the vapor) and H_{peb} (for the pebbles), respectively.
2.5.1. Singleseed pebble model
In the singleseed model, we follow the vapor surface density Σ_{Z}, the ice surface density Σ_{ice}, and the number density of particles N_{p}. The equations governing the time evolution of these quantities are: where the source terms and are defined in Eqs. (12) and (15), ℳ_{ice} and ℳ_{Z} are the ice and vapor mass flux, respectively, and is the number flux of solid particles. These fluxes are given by:
where v_{peb} is the drift velocity of the pebbles given by Eq. (8) or by Eq. (B.7) when including collective effects, N_{gas} is the number of gas particles, and D_{p} is the particle diffusivity, which is related to D_{gas} through the Schmidt number Sc (Youdin & Lithwick 2007): (23)Since in our models the stopping times are much smaller than unity, we set D_{p} equal to D_{gas}.
Note that a negative flux means that material is transported inwards, towards the star. Under the singlesize approximation, the typical pebble mass m_{p} is given by: (24)with m_{core} the mass of the bare silicate cores of the pebbles.
2.5.2. Manyseeds pebble model
We implement the manyseeds model as follows. We now consider two additional populations of solids: dirt and free silicates. Dirt refers to the silicates that are captured in icy pebbles, whereas free silicates are small silicate grains without any ice coating. The transport equations for Σ_{ice}, Σ_{Z}, and N_{p} are the same as in the singleseed pebble model (Eqs. (17)–(19)). The transport equations for the dirt surface density Σ_{dirt} and free silicates surface density Σ_{sil} are given by: where ℳ_{dirt} and ℳ_{sil} are the dirt and free silicate mass fluxes, respectively. Free silicates are released from the pebbles at a rate proportional to the decrease of ice surface density due to evaporation and to the amount of dirt that can evaporate from within the pebbles: (R_{e} − R_{c}Σ_{vap})Σ_{dirt}, but only when there is net evaporation of ice. Silicate grains stick to icy pebbles at a collision/sticking rate R_{s}: (27)where Δv_{sil,peb} is the relative velocity between the pebbles and the silicates and H_{sil} is the scale height of the free silicates. Since the inward drift velocity of the pebbles is much larger than the outward diffusion velocity of the silicates, we take Δv_{sil,peb} ≈ v_{peb}^{2}.
The dirt and silicate mass fluxes, ℳ_{dirt} and ℳ_{sil}, are given by:
where v_{peb} is again the radial drift velocity of the pebbles, and silicates are advected with the gas.
2.6. Effects of variable μ
When icy pebbles evaporate, the gas becomes enriched in water vapor. This means that the mean molecular weight μ of the gas increases: (30)where f_{H2O} is the mass fraction of water molecules, μ_{H2O} = 18m_{H} is the mean molecular weight of water, and f_{gas} is the mass fraction of gas molecules (without the vapor contribution), with μ_{gas} = 2.34m_{H}.
Since the sound speed c_{s} is proportional to , the sound speed decreases as more water vapor is added. The disk scale height H_{gas} is proportional to c_{s} and will therefore decrease as well: the disk becomes more vertically compact with increasing water vapor. An increase in μ across the water evaporation front has an effect on the pebble drift velocity v_{peb} (Eq. (8)) in this region, since v_{peb} is proportional to 1 /μ through its dependence on c_{s}, and sensitive to variations in the gas pressure P through ∂log P/∂log r. The total gas pressure (hydrogen/helium plus water) is given by: (31)We take the viscosity ν to be independent of variations in μ. Therefore, Σ_{gas} = Ṁ_{gas}/ 3πν is independent of μ as well. However, the H_{2}Oenriched gas is characterized by a reduced scaleheight, since , increasing the midplane gas pressure P_{gas} as . Evaporation hence increases the pressure gradient and the headwind of the gas through Eq. (9): pebbles tend to drift faster. Finally, the drift velocity v_{peb} also depends on the stopping time τ_{S}, which in turn depends on the gas density and the thermal velocity – both quantities that depend on μ. We take these dependencies into account as well.
We now define two models that we study in the following sections. In the simple model, we do not include collective effects and the variability of the mean molecular weight μ. In the simple model, the sound speed and scale height are independent of variations in μ, ηv_{K} (Eq. (9)) is constant and the midplane gas density is μindependent: . In the complete model, we do take collective effects and variations of μ into account, as described above.
2.7. Input parameters
The four key input parameters that can be varied in our model are:

The gas accretion rate Ṁ_{gas}.

The ratio between the pebble accretion rate and the gas accretion rate, denoted by the symbol ℱ_{s / g}, and defined as: (32)

The dimensionless turbulence parameter α.

The initial stopping time of pebbles just outside the snowline (at 3 au) denoted by the symbol τ_{3}. This parameter is simply a proxy for the mass of the incoming pebbles.
Together, these input parameters define the “zeromodel” of the disk: the gas and solids distribution in the case of no condensation and evaporation. The gas surface density profile Σ_{gas} is defined through Eq. (4), where the turbulent viscosity ν is determined by α through Eq. (5). With Σ_{gas} and the stopping time normalization τ_{3} at 3 au, we can find τ(r) at any other radius r. We can then also determine the pebbles surface density Σ_{peb} for the zeromodel: it is given by ℱ_{s / g}Ṁ_{gas}/ 2πrv_{peb}(r), where the pebble velocity v_{peb}(r) depends on τ(r) and is given by Eq. (8) (without backreaction) or Eq. (B.7) (including backreaction).
2.8. Model assumptions
In constructing our model we employed several assumptions, which we discuss below.

We do not include a particle size distribution, but rather considerone typical pebble size at each time and location in the disk. In themanyseeds model, we do distinguish between the population ofsmall silicate grains and large icy pebbles, however. We comeback to the importance of condensation onto small grains ratherthan onto pebbles in the discussion (Sect. 6).

Our model does not account for coagulation among pebbles: the enhancement of the solidstogas ratio is solely due to diffusion and condensation. We remain agnostic as to what happens to the pebbles in terms of coagulation and fragmentation until they reach the evaporation front. In the manyseeds model, we do not take into account coagulation of silicate particles. We will come back to this point in the discussion (Sect. 6).

Our model is 1D, and has a straight vertical snowline. In reality, the vertical snowline is curved rather than straight, because the temperature varies with height above the midplane (e.g., Oka et al. 2011). However, Ros & Johansen (2013) have shown that particle growth due to diffusion and subsequent condensation of water across the vertical snowline is negligible compared to the same process across the radial snowline.

Similarly, we assume that the scale height of the vapor – and, in the manyseeds implementation, of the free silicates – is always equal to the scale height of the disk; in other words, when an icy pebble evaporates, the released water vapor immediately distributes itself over the same vertical extent as the background gas, whereas it originates from the icy pebbles that reside in a thinner disk, characterized by a scale height H_{peb}: (33)The assumption of rapid vertical mixing extends to the calculation of the mean molecular weight of the gas in the complete model. Also there, it is assumed that the water vapor is distributed evenly throughout the gas at all times. In Sect. 4.2, we verify that the assumption of taking the vapor scale height equal to the disk scale height rather than the pebbles scale height, does not have a large effect on the results.

We assume a steadystate gas distribution, that is, Ṁ_{gas} and T remain constant. This assumption is justified since the solidstogas enhancement takes place on a radial scale Δr that is small compared to the size of the disk. In other words, the local viscous evolution timescale (Δr^{2}/ν), on which the effect happens, is much smaller than the global viscous evolution timescale of the disk, on which the gas accretion rate and global temperature profile change. The temperature profile (Eq. (1)) corresponds to a passivelyirradiated disk. However, in case of viscous heating T(r) will still be described by a powerlaw (Armitage 2015). We have checked the effect of adopting a viscous heating temperature profile (T(r) ∝ r^{− 3 / 4}) in our numerical simulation. The key consequence is that the location of the snowline is shifted in radius; all other model results are very similar.

We adopt an αviscosity model, with constant α (the value of which we allow to vary between very high and very low values), independent of the solidstogas ratio. However, if turbulence is driven by the magnetorotational instability, the local turbulence strength at the midplane depends on the local grain size and abundance. Socalled “dead zones”, where turbulence is strongly reduced, could occur at locations in the disk with a sharp increase in the solidstogas ratio (Kretke & Lin 2007). Since our results depend strongly on the amount of turbulence near the snowline, the creation of dead zones would change our results.

Similarly, we do not consider the interplay between (small) grains and the local temperature: we do not solve for the temperature profile selfconsistently, but take it as constant, given by Eq. (1). However, in the manyseeds model, a large amount of small silicate grains is released in the evaporation front. This means that locally the opacity could increase. Conceivably, this could lead to a steeper temperature profile in the region near the snowline and therefore to a more narrow evaporation front. Including these effects requires a radiation transfer model, which is beyond the scope of this work.

In the manyseeds implementation, we do not include condensation onto the small, free silicate particles. We also do not model the porosity of pebbles. We come back to these issues in Sect. 6.3.
Fig. 2
The solution to the transport equations at different points in time, for the fiducial model parameters listed in Table 1. At t = 10^{5}yr, approximately 90% of the steadystate peak in the ice surface density has formed. a) Surface densities Σ of ice (solid lines) and vapor (dashed lines). The dotted line corresponds to the steadystate advectiononly vapor surface density profile. b) Midplane pebblestogas ratio ρ_{peb}/ρ_{gas}. c) Typical pebble mass m_{p}. d) Typical pebble internal density ρ_{•,p}. 
3. Numerical implementation
We make use of the open source partial differential equations solver FiPy (Guyer et al. 2009) to solve the transport equations numerically. The coupled systems of equations are solved on a cylindrical 1D grid that ranges from 1 to 5 au.
We implement boundary conditions as follows. At the outer boundary r_{2} = 5 au, the pebble mass flux ℱ_{s / g}Ṁ_{gas} is fixed^{3}. We convert the input parameter τ_{3} to a physical pebble size s_{p,start} using Eq. (7), and since our model does not include coagulation, we set the pebble size (which can be converted to a pebble mass m_{p,start}) at the outer boundary r_{2} to this value. For the singleseed model, the mass of the bare silicate core is then given by m_{core} = ζm_{p,start} = m_{p,start}/ 2. At the inner boundary r_{1} = 1 au, we implement outflow boundary conditions: solid particles and water vapor are accreted to the central star at a constant rate. We also demand that Σ_{ice} = 0 at r_{1} and Σ_{Z} = 0 at r_{2}, for obvious reasons. Additionally, in the manyseeds implementation we have Σ_{dirt} = Σ_{ice} = 0 at r_{1} and Σ_{sil} = Σ_{Z} = 0 at r_{2}.
3.1. Timedependent
In our timedependent method, we adopt small time steps (Δt ~ 100yr) and a small value for the allowed residuals, to ensure mass conservation by demanding the residuals^{4} to be small. This method requires a lot of computational power because the system of partial differential equations is numerically very stiff, but the advantage is that we find not only the steadystate solution to the equations, but are able to follow the solution in time. This allows us to get a measure of the time needed for the solution to settle into a steadystate. We present the timedependent results for the “simple, singleseed” model with fiducial input parameters in Sect. 4.1.
3.2. Timeindependent
Our timeindependent method solves for the steadystate solution directly, by taking very large timesteps (in total 40 time steps that increase to 10^{7}yr) and decreasing the residuals threshold after each run, taking the solution from the previous run as the new input. We continue this process until we reach convergence. We present the steadystate results for the “simple, singleseed”, “simple, manyseeds”, “complete, singleseed”, and “complete, manyseeds” models with fiducial input parameters in Sect. 4.2.
4. Results – fiducial model
In this section we introduce a standard set of parameters which we then use to illustrate different aspects of the model. The fiducial model is defined by the parameters listed in Table 1. We first discuss the timedependent results for the simple, singleseed, fiducial model in Sect. 4.1. We then go on to discuss the steadystate results for the other variants of the fiducial model in Sect. 4.2.
Fiducial model parameters.
4.1. Timedependent solution
In Fig. 2 we plot several quantities as function of radial distance from the star r, at four points in time. In Fig. 2a, the surface densities of ice (solid lines) and vapor (dashed lines) are plotted. Initially (t = 0), the ice and vapor surface density are zero, Σ_{ice} = Σ_{Z} = 0. Icy pebbles are drifting in from the outer disk (right) to the inner disk (left). At the point where the icy component of the pebbles evaporate. At the snowline r_{snow} ≈ 2.1 au all the H_{2}O is in the gas phase. Since the vapor is advected with the gas velocity v_{gas}, which is much smaller than the pebble velocity v_{peb}, the vapor surface density (dashed line) quickly exceeds that of the ice (solid line). The vapor density increases until the steadystate vapor distribution Σ_{Z,a} has been reached. Σ_{Z,a} is given by^{5}: (34)and is plotted by the dotted curve. Meanwhile, due to the outward diffusion of water vapor across the snowline and subsequent condensation onto the inwarddrifting pebbles, the ice surface density just exterior to the snowline increases. Diffusion of vapor therefore results in a distinct bump in the ice profile and we denote the location corresponding to maximum Σ_{ice} the peak radius r_{peak}. A similar maximum is seen in the solidstogas ratio (Fig. 2b), which rises to ~0.45. After t = 2 × 10^{5} yr a steady state has been reached.
The enhancement of the pebblestogas ratio is reflected by the typical pebble mass m_{p} and density ρ_{•,p}, plotted in Figs. 2c and d, respectively. Pebbles at the inner boundary are half as massive as pebbles at the outer boundary, because at the inner boundary all the ice has evaporated off the pebbles, and the dust fraction of pebbles ζ = 0.5. The typical pebble mass just outside the snowline increases over time, indicating that water vapor condenses onto the pebbles. This is also shown by the behavior of the typical pebble density ρ_{•,p}. At the outer boundary, ρ_{•,p} = 1.5gcm^{3}, corresponding to pebbles containing as much water ice as silicates in mass; at the inner boundary, ρ_{•,p} = 3gcm^{3}, corresponding to pure silicate pebbles; whereas just outside the snowline, ρ_{•,p} decreases over time to values close to unity – corresponding to pure water ice pebbles. A decrease in particle internal density outside the snowline due to water condensation was also found by Estrada et al. (2016).
Fig. 3
Rate of change of the ice surface density at the peak location, as function of time. The rate of change increases until the icy pebble front has reached the peak location, after which the peak continues to grow at an exponentially decreasing rate, while the system is converging to its steadystate solution. 
In Fig. 3 we plot the growth rate of the peak in Σ_{ice} outside the snowline as function of time t. At the start of the simulation, ice is not yet present at the location of the peak. After the icy pebbles have reached the location of the eventual peak, at t ~ 2 × 10^{4}yr, the rate of growth decreases exponentially – the peak continues to grow, but at an ever slower rate, while the system is converging to its steadystate solution. The efolding growth timescale is ~3 × 10^{4}yr, which is approximately equal to the gas advection timescale (r_{peak} − r_{snow}) /v_{gas}; the time it takes for the vapor to traverse the peak and contribute to the steep vapor concentration gradient along which outward diffusion can take place. We will come back to the peak formation timescale in Sect. 5. The time in which 90% of the peak forms is ~10^{5}yr. Note that we have assumed that the incoming pebble mass flux does not change over time (ℱ_{s / g} is constant at the outer boundary r_{2}). If the pebble flux would decrease on a timescale shorter than the time it takes to form the peak, a steadystate would not exist. If the pebble flux would decrease on a timescale longer than it takes to form the peak, we would reach a quasisteadystate solution; in that case our model is fully applicable.
Fig. 4
Steadystate results for the fiducial parameters, for the simple model with singleseed evaporation (upper two panels) and manyseeds evaporation (lower two panels). a) Surface densities of ice, silicates and vapor (Σ_{ice}, Σ_{sil}, and Σ_{Z}, respectively) for the singleseed model. The silicates are locked in the icy pebbles outside the snowline, whereas they are bare grains interior to the snowline. b) Midplane pebblestogas ratio ρ_{peb}/ρ_{gas}, and pebblestogas column density ratio Σ_{peb}/ Σ_{gas} for the singleseed model. c) Same as panel a) but for the manyseeds model. The silicates are now divided in two populations: silicates that are locked up in icy pebbles (Σ_{dirt}), and free silicates (Σ_{sil}). Note that in panels a) and c) the xaxis ranges between r = 1.8 − 2.8au, for clarity. d) Same as b), but for the manyseeds model and with an additional line for the midplane “free silicates”togas ratio ρ_{sil}/ρ_{gas}. 
4.2. Steadystate solution
The timedependent solution described in Sect. 4.1 converges to the steadystate solution. In this section we take a closer look at the steadystate solution for the fiducial parameters, for the model designs discussed in Sect. 2.
4.2.1. Singleseed versus manyseeds
In Fig. 4 we compare the simple singleseed model (upper two panels) with the simple manyseeds model (lower two panels). The left panels show the surface densities of ice, vapor, and in the manyseeds case, also of locked silicates (dirt) and free silicates. The ice profiles are very similar in both models, but in the manyseeds case there is an additional peak in the dirt surface density. This is because the free silicates behave like vapor: they are released throughout the evaporation front, and follow the gas profile interior to the snowline. Turbulent diffusion not only causes vapor to be transported outward and condense onto the pebbles, but leads to the same effect for the small silicates – they diffuse outward and stick onto the pebbles, resulting in a peak in the dirt surface density distribution.
In the right panels we plot pebblestogas midplane density ratios ρ_{peb}/ρ_{gas} and column density ratios Σ_{peb}/ Σ_{gas}. In the manyseeds model, the pebblestogas ratio is the sum of the dirttogas ratio and the icetogas ratio. In both models, a clear peak is present just outside the snowline. The midplane density ratio is larger than the column density ratio due to settling of pebbles. In the manyseeds case, we also plot the free silicatestogas midplane density ratio ρ_{sil}/ρ_{gas}. This ratio is constant interior to the snowline because the silicates are perfectly coupled to the gas. In the manyseeds model, small silicate grains diffuse outward across the snowline, whereas in the singleseed model, there is no significant outward diffusion of the larger silicate pebbles due to the absence of a steep concentration gradient. Therefore, the peak in the pebblestogas ratio outside the snowline is larger in the manyseeds model than in the singleseed model.
4.2.2. Simple versus complete models
Figure 5 shows the results for the complete model with the singleseed pebble design (upper two panels, a and b) and with the manyseeds pebble design (lower two panels, c and d). In Fig. 5a (singleseed) and Fig. 5c (manyseeds), we plot the surface densities of ice, vapor, and in the manyseeds case the surface densities of locked silicates (dirt) and free silicates (sil). Dashed lines denote the simple model results of Figs. 4a and c, for comparison. The grey lines correspond to the mean molecular weight of the gas. From the outer disk to the inner disk, the mean molecular weight increases from 2.34 m_{H} to 3.11 m_{H} across the snowline. Clearly, the peak in the ice surface density is higher and broader for the complete model than for the simple model. This is because collective effects (which reduce the pebble drift velocity) outweigh the effect of the enhanced gas pressure gradient in the evaporation front (which enhances the pebble drift velocity). In the complete model, therefore, pebbles effectively have a smaller radial velocity than in the simple model, and therefore the resulting ice peak is higher and broader. This is also the case in the manyseeds implementation. The width of the peak strengthens the justification of the vertical mixing assumption (see below).
In Figs. 5b and d we compare the midplane pebblestogas ratios between the simple and the complete model. Collective effects help to boost the pebblestogas ratio, for the reason outlined above.
Fig. 5
Comparison of steadystate results for the fiducial parameters between the simple model (dashed lines) and the complete model (solid lines), which includes collective effects and the effects of the variation of the mean molecular weight μ. The upper two panels correspond to the singleseed evaporation model; the lower two panels correspond to the manyseeds evaporation model. In the latter case, we made the conservative choice of not including the free silicates in the backreaction onto the gas. a) Surface densities of ice (Σ_{ice}), vapor (Σ_{Z}) and silicates (Σ_{sil}) for the singleseed model. The grey line indicates the mean molecular weight of the gas in units of proton mass m_{H}. b) Midplane pebblestogas ratio ρ_{peb}/ρ_{gas}. c) Same as a), but the silicates are now divided into “free silicates” (Σ_{sil}) and “locked silicates” (Σ_{dirt}). For clarity, we only show the clean Σ_{ice} profile for comparison. d) Same as b), with an additional line denoting the “free silicates”togas ratio ρ_{sil}/ρ_{gas}. 
4.2.3. Validation of vertical mixing assumption
As discussed in Sect. 2.8, we assume rapid vertical mixing of vapor. However, it could be argued that (part of) the released vapor recondenses onto icy pebbles before relaxing to the same vertical distribution as the gas, thereby boosting the condensation rate. This assumption also extends to the small silicate grains in the manyseeds model. Similarly, one could argue that the silicate grains can collide with a pebble before they can diffuse to higher vertical layers (e.g., Krijt & Ciesla 2016). In order to investigate what the difference is in terms of the steadystate ice distribution between two extreme cases, we take the simple, singleseed, fiducial model and run it once with H_{Z} = H_{gas} and once with H_{Z} = H_{peb}. We compare the steadystate outcomes of the two cases in Fig. 6. Even though the location of the snowline and of the pebblestogas peak differs a bit between the two cases, the height of the peak in the midplane pebblestogas ratio increases only by ~0.3% if one takes H_{Z} = H_{peb} instead of H_{Z} = H_{gas}. Similarly, assuming a smaller scale height for the silicate grains in the evaporation region would probably not significantly change the height of the peak in the “locked” silicates, since the silicate grains behave like vapor. In the rest of this paper, we assume H_{Z} = H_{sil} = H_{gas}.
Fig. 6
Comparison of steadystate results for the simple, singleseed, fiducial model between the case where vapor has the same vertical distribution as the background gas (H_{Z} = H_{gas}) and the case where vapor has the same scale height as the pebbles (H_{Z} = H_{peb}). In all three panels, solid lines correspond to the H_{Z} = H_{gas} case and dashed lines correspond to the H_{Z} = H_{peb} case. a) Steadystate water ice (blue) and water vapor (green) surface densities. b) Midplane solidstogas ratios (green) and solidstogas surface densities ratios (blue). c) Typical pebble mass m_{p}. 
5. Streaming instability conditions
Fig. 7
a) Contours of constant relative ice surface density peak heights f_{Σ,peak} (see text for details) as function of turbulence parameter α and solidstogas accretion rate ℱ_{s / g}. The gas accretion rate Ṁ_{gas} is fixed to 10^{8}M_{⊙}yr^{1} and the initial size of the pebbles τ_{3} is fixed to 0.03. b) Contours of constant relative ice surface density peak heights (see text for details) as function of the turbulence parameter α and the gas accretion rate Ṁ_{gas}. The solidstogas accretion rate ratio ℱ_{s / g} is fixed to 0.4 and the initial size of the pebbles τ_{3} is fixed to 0.03. The cyan lines denote a Toomre parameter (Q_{T}) of unity at 10 au (1 au); the space below these lines has Q_{T}< 1 and is gravitationally unstable at 10 au (1 au). 
Carrera et al. (2015) have investigated for what values of the solidstogas column density ratio streaming instability occurs, as function of the stopping time of the solid particles. They found that, typically, the solidstogas column density ratio should exceed ~2% for stopping times ~5 × 10^{2}. However, these results should be interpreted with caution, since Carrera et al. (2015) only accounted for selfdriven (KelvinHelmholtz) turbulence. We do include global turbulence, and therefore cannot simply use their conditions for streaming instability. A more robust condition for streaming instability in the presence of global turbulence is probably a midplane solidstogas ratio that reaches order unity (Johansen & Youdin 2007).
In this section we investigate under what disk conditions, the midplane solidstogas ratio near the snowline gets most enhanced due to the effect of water diffusion and condensation. To this end, we have constructed a semianalytic approximate model to be able to quickly test for many different values of the input parameters (Sect. 2.7), within the singleseed implementation (Sect. 2.4). Before presenting the results, we will provide a short summary of the semianalytical model, which is discussed in greater detail in Appendix C.
5.1. Semianalytical model: Summary
Our semianalytical model is an analytic prescription to find the approximate location, height and width of the ice surface density at the location of the ice peak, r_{peak}, of the steadystate (timeindependent) solution (see Sect. 3.2 for our numerical method to find the steadystate solution to the transport equations). For simplicity, we have tailored the semianalytical model towards the “singleseed” design. (An extension to also include the “manyseeds” design will be considered in a future work.)
The model works by iteratively solving a set of analytical equations, until convergence is reached. The key parameter is the ratio between the pebble velocity at r_{peak} and the normalized diffusivity at this location, ϵ = v_{peb}(r_{peak}) /D(r_{peak})r_{peak}. Initially, we start with an estimate for ϵ, which can, for example, be taken from the zeromodel solution (Sect. 2.7). For a certain ϵ the semianalytical model then updates the surface density at the peak (Σ_{peak}) as well as r_{peak} (or rather the difference between r_{ice} and r_{peak}). With these updates we obtain a new value of ϵ and the procedure can be repeated until the fractional change in the parameters has become sufficiently low.
We emphasize that the semianalytical model gives approximate solutions (correct at the ~20% level), but that they are very useful since they come at almost zero computational costs. It is therefore ideal to be applied to the parameter searches that we consider in this section. In Appendix C the model is described in detail and compared to runs of the numerical steadystate model.
5.2. Enhancement of the ice surface density
We first look at the relative effect of enhancing the ice surface density near the snowline: for each disk model, we normalize the resulting peak ice surface density by the ice surface density at the peak radius in case there is only advection: (35)where v_{peb} is calculated in the absence of condensation and evaporation. As before, we take ζ = 0.5. In Fig. 7a we plot contours of constant f_{Σ,peak} as function of α and ℱ_{s / g}, where Ṁ_{gas} is fixed at 10^{8}M_{⊙}yr^{1} and τ_{3} is fixed at 0.03. Clearly, the higher the solidstogas accretion rate ℱ_{s / g}, the higher f_{Σ,peak} – at fixed α the normalized ice peak increases from low ℱ_{s / g}values to high ℱ_{s / g}values, due to collective effects playing an increasingly important role. The plot also shows that disks with αvalues of about 10^{3} are best at enhancing the ice surface density with respect to the advectiononly expected ice surface density. This is because higher values of α lead to a broader and relatively lower peak, while lower αvalues, indicating larger gas densities, move pebbles into the Stokes drag regime. The fact that the relative height of the ice peak becomes smaller when pebbles enter the Stokes regime, is explained by the pebble sizedependency of the drift velocity. In the Epstein regime the drift velocity depends linearly on the pebble size, whereas in the Stokes regime the drift velocity is proportional to the square of the pebble size. This means that when pebbles enter the Stokes regime, their stopping time – and hence their drift velocity – increases rapidly. The effect of this is that f_{Σ,peak} decreases rapidly. Therefore, the transition from the Epstein regime to the Stokes drag regime is characterized by closelyspaced contours.
Figure 7b shows contours of constant f_{Σ,peak}, as function of α and Ṁ_{gas}. ℱ_{s / g} is fixed at 0.4 and τ_{3} is fixed at 0.03. The cyan lines correspond to a Toomre parameter (Q_{T}) of unity at 10 au (1 au). Q_{T} is defined as: (36)where G is the gravitational constant. A disk is gravitationally unstable if Q_{T}< 1. In Fig. 7b, models in the parameter space below the cyan line have Q_{T}< 1 at 10 au (1 au). In Fig. 7b denselyspaced contours again indicate the transition between Epstein and Stokes drag.
The enhancement of the ice surface density near the snowline is relatively modest, but enrichment factors of a few can still be important for triggering streaming instability (Johansen et al. 2009). Besides, Fig. 7 corresponds to our singleseed model, which is conservative. Larger enhancements can be achieved in the framework of the manyseeds model (see Fig. 4). We can imitate the manyseeds model in the analytical model of Appendix C, crudely, when we let ζ → 0, which assumes that micronsized silicate grains behave like vapor. In that case we see f_{Σ,peak} increase by another factor of two (results not plotted). Therefore, total enhancements of f_{Σ,peak} ~ 5–10 are feasible, which significantly boost the likelihood of triggering streaming instability.
Fig. 8
a) Contours of midplane solidstogas ratios (black) as function of the turbulence parameter α and the solidstogas accretion rate ℱ_{s / g}. The gas accretion rate Ṁ_{gas} is fixed to 10^{8}M_{⊙}yr^{1} and the initial size of the pebbles τ_{3} is fixed to 0.03. Orange contours denote the amount of solid material (in Earth masses) that is required to form the eventual peak in the ice surface density just outside the snowline. b) Contours of midplane solidstogas ratios as function of α and Ṁ_{gas}. The solidstogas accretion rate ℱ_{s / g} is fixed to 0.4 and the initial size of the pebbles τ_{3} is fixed to 0.03. Orange contours denote the amount of solid material (in Earth masses) that is required to form the eventual peak in the ice surface density just outside the snowline. The cyan lines denote a Toomre parameter (Q_{T}) of unity at 10 au (1 au); the space below these lines has Q_{T}< 1 and is gravitationally unstable at 10 au (1 au). 
5.3. Solidstogas ratios
Let us now look at the absolute results, in terms of the midplane solidstogas ratio. In Fig. 8a, black lines denote contours of constant peak midplane solidstogas ratios, as function of α and ℱ_{s / g}. We again fix Ṁ_{gas} = 10^{8}M_{⊙}yr^{1} and τ_{3} = 0.03. The orange contours correspond to the total amount of solids in units of Earth masses that is needed to form the eventual peak. This quantity (M_{solids,needed}) is calculated as: (37)where (r_{peak} − r_{snow}) /v_{gas} is the typical timescale on which the peak forms, as discussed in Sect. 4.1. The value of M_{solids,needed} is similar to the amount of solids that gets “locked up” in the peak^{6}. Figure 8a shows that the higher the value of ℱ_{s / g}, the easier streaming instability can be triggered, as one may expect. It also shows that in order to reach midplane solidstogas ratios of ~10%, a solidstogas accretion rate ℱ_{s / g} of the same order is required. This also holds for other values of the gas accretion rate Ṁ_{gas} and initial pebble size τ_{3}.
Figure 8b is the same as Fig. 7b, except that the black contours now denote constant values of the peak midplane solidstogas ratio. Just like in Fig. 8a, orange contours denote constant M_{solids,needed}, but now with Ṁ_{gas} as the parameter on the xaxis. The region with closelyspaced contours in Fig. 8a and the oblique regions in the otherwise fairly horizontal contours in Fig. 8b are again due to the transition between the Epstein and Stokes drag regimes.
Up to this point we have kept the parameter τ_{3} constant at its fiducial value of 0.03. Recently, Yang et al. (2016) have shown that the streaming instability mechanism can also work for small particles (τ ~ 10^{3}). In Fig. 9 we now vary τ_{3} and plot the resulting peak midplane solidstogas ratio, whilst fixing Ṁ_{gas} at 10^{8}M_{⊙}yr^{1}, ℱ_{s / g} at 0.4, and α at 3 × 10^{3}. Different regimes in the plot are denoted by Roman numbers I–IV. In region I, the particles are wellcoupled to the gas. The solidstogas ratio flattens out towards low τ_{3}values, because radial drift and settling do not play a role for these particles. The boundary between regime I and regime II corresponds to the value of α. The highest solidstogas ratios are reached for particles with stopping times of the same order as α or smaller. For higher values of τ, the larger drift velocity (proportional to τ) starts to dominate over the larger degree of settling (proportional to ). Therefore, in regime II, the solidstogas ratio decreases with increasing τ. The transition from regime I and regime II corresponds to the τ_{3}value for which ϵ is unity. The ϵ parameter (introduced in Sect. 5.1) increases with increasing τ_{3}, and the peak surface density decreases at a faster rate with increasing ϵ for ϵ> 1 than for ϵ< 1 (Eq. (C.13)). The physical explanation is that the solution changes from diffusiondominated (ϵ< 1) to driftdominated (ϵ> 1). Therefore, the solidstogas ratio decreases more steeply in regime III than in regime II. The final transition, from regime III to regime IV, is caused by the transition from the Epstein regime to the Stokes regime. For τ_{3} values of ~1, the enhancement effect becomes minimal and the peak solidstogas ratio flattens out.
Fig. 9
Peak midplane solidstogas ratio as function of τ_{3}. Ṁ_{gas} is fixed at 10^{8}M_{⊙}yr^{1}, ℱ_{s / g} at 0.4, and the value of α is 3 × 10^{3}. We can distinguish four regimes I–IV, which are explained in the main text. 
From Figs. 8a and b we learn that in the context of the αviscosity disk model, the largest solidstogas ratios near the snowline are reached for high αvalues. This means that our diffusion model does not require a very quiescent disk to achieve high solidstogas ratio, and also works in the early disk phase when α and Ṁ_{gas} are presumably high. Our results show that for high α and high Ṁ_{gas}, tens of Earth masses are locked up in pebbles in an annulus outside the snowline with a width of the order of 1 au.
6. Discussion
6.1. Conditions for streaming instability
Our results show that the ice surface density can be enhanced by a factor ~3–5 outside the snowline, due to the effect of water diffusion and subsequent condensation onto icy pebbles (adopting ζ< 0.5 or the manyseeds model increases the enhancement by another factor ~2). This differs from the results of Stevenson & Lunine (1988), who found that the same effect could lead to an enhancement by as much as 75. However, they considered a static system, whereas our model accounts for radial drift of pebbles and gas accretion onto the star. Even though we found a modest enhancement, we showed that the pebble density at the midplane can reach tens of percent of the gas density, under the condition that the solidstogas accretion rate ℱ_{s / g} is of order 0.1.
But what are realistic values for ℱ_{s / g}? Ida et al. (2016) have calculated the pebble mass flux Ṁ_{peb} in a viscouslyevolving disk, taking into account dust growth and radial drift. They found that after 10^{6} yr, ℱ_{s / g} ~ 0.3 for a turbulence parameter α = 10^{3} and a gas accretion rate Ṁ_{gas} = 10^{8}M_{⊙}yr^{1}. Since this result suggests ℱ_{s / g}values of order 0.1 are plausible, water condensation can plausibly trigger streaming instability near the snowline. According to Ida et al. (2016), Ṁ_{peb} is inversely proportional to α. This implies that even though our results show that for high αvalues, water diffusion and condensation leads to the largest solidstogas ratio at the snowline, a smaller pebble mass flux is expected, which reduces the effect. The pebble mass flux is, however, dependent on time t as Ṁ_{peb} ∝ t^{− 1 / 3}, meaning that the pebble mass flux earlier in the disk is higher than the fiducial 30% of the gas accretion rate quoted before. Because higher αvalues lead to larger solidstogas ratios but to lower pebble mass fluxes, we conclude that intermediate αvalues (~10^{3}) are most favorable to trigger streaming instabilities. The fact that the diffusiondriven model of this work already produces enhancement of solids at intermediate αvalues and high Ṁ_{gas}, implies that planetesimal formation does not have to await the arrival of quiescent disk conditions. Provided a sufficiently large pebble flux, our results imply that planetesimals can form early.
6.2. Interior or exterior?
In Saito & Sirono (2011), it is argued that the evaporation of icy pebbles leads to a large enhancement of small silicate grains interior to the snowline. In their model, micronsized silicate grains are instantaneously released at the snowline, and then follow the radial motion of the gas. Since the gas moves at a much lower velocity than the drift velocity of the icy pebbles, the silicate grains pileup and become gravitationally unstable. A similar mechanism for the formation of planetesimals in the inner disk has recently been presented by Ida & Guillot (2016).
We confirm that the solidstogas ratio interior to the snowline is boosted due to the slow radial motion of the small silicates (see Fig. 4c), but find smaller enhancements than Saito & Sirono (2011) and Ida & Guillot (2016). These works assumed that the evaporated silicate grains remained in the same vertical layer as the icy pebbles, which had settled to the midplane due to their larger size. This is a natural assumption if one adopts instantaneous evaporation. However, in our model silicate grains are not instantaneously released from the pebbles at a single location, but are instead released across the ice evaporation front – the region between the snowline and the peak radius. With the exception of very low αvalues, the width of the ice peak is (much) larger than the gas scale height. Consequently, the timescale for vertical mixing is smaller than the timescale on which the silicate grains traverse the evaporation front, justifying our assumption that silicate grains (and water vapor) are distributed over H_{gas}. Allowing for the vertical mixing of silicate grains is why we found smaller solidstogas ratios interior to the snowline than Saito & Sirono (2011) and Ida & Guillot (2016).
In this work we did not model the porosity of pebbles, but assumed pebbles are compact spheres. For homogeneous porous spheres, the results are the same as for compact spheres with the same stopping time, if they are in the Epstein regime. This is because the evaporation and condensation rates (Eqs. (13), (14)) depend on (the surface to mass ratio of a pebble), which is effectively the Epstein stopping time (Eq. (7)). For fractal aggregates, however, the evaporation rate could conceivably be increased due to a larger total surface area available for evaporation. In that case, the location of the snowline (r_{snow}) and of the peak (r_{peak}) are pushed to larger radial distances, because drifting pebbles start to evaporate earlier. The shape of the solids distribution profile and hence the width of the evaporation front, however, remain similar. We have confirmed this behavior by running our simulation with an evaporation rate that has been arbitrarily increased by a factor 100 compared to Eq. (13). Therefore, a fractal interior structure of the pebbles would not much change the extent of the region in which pebbles evaporate. We note however that in the manyseeds model, a large increase in opacity due to small silicate grains might lead to a steeper temperature profile than assumed here, and therefore to a more narrow evaporation front.
Even though we found smaller enhancements interior to the snowline, adopting the manyseeds model leads to larger enhancements outside the snowline compared to the singleseed model. This is because outward radial diffusion and subsequent sticking of silicate grains to icy pebbles adds to the ice peak and therefore enforces the enhancement of the solidstogas ratio outside the snowline (see Fig. 5).
6.3. Condensation onto small grains
In our singleseed model, we adopted a singlesize assumption for the solid particles, applicable to a driftlimited scenario, in which particles grow until they decouple from the gas and start to drift inward (see, e.g., Birnstiel et al. 2010; Krijt et al. 2016b). Because the solids density is larger close to the star than in the outer disk, particles close to the star start to drift inward earlier than particles in the outer disk. This leads to an insideout clearing of the solids component of the disk. In this case, one would not expect small particles to be present in significant amounts near the snowline at the time when icy pebbles approach the snowline, drifting in from the outer disk. Therefore, in the driftlimited case the singlesize approximation for pebbles is valid.
The singlesize assumption does not hold for a fragmentationlimited size distribution, however. In that case, pebbles dominate the total mass of solids, but small particles dominate the total surface area (see, e.g., Birnstiel et al. 2012). Then, condensation of water vapor will predominantly happen onto small particles, instead of onto pebbles as considered in this work. Also, in our manyseeds model, we do not allow for condensation onto the small grains that get released from icy pebbles upon evaporation.
Within the singleseed framework, we can mimic the situation where condensation happens onto small grains rather than onto pebbles by adopting a very small typical stopping time just outside the snowline (τ_{3}). This results in approximately the same or even larger peaks, as illustrated by Fig. 9. In that sense, assuming condensation occurs solely onto pebbles, rather than onto small grains, is a conservative choice. However, a more correct approach would allow for condensation onto small grains in the manyseeds model, in which icy pebbles break up into small grains upon evaporation, or, alternatively, within a fragmentationlimited scenario by adopting a full size distribution. Such improvements will be considered in future work.
6.4. Relevance of coagulation
The manyseeds model ignores coagulation among the small silicate grains, as well as the possibility that water vapor condenses on to silicates. Because there are so many of them, the average silicate grain size would not increase significantly due to water condensation. In that case, the assumption that they are wellcoupled to the gas would still hold. However, growth of silicates might also occur due to coagulation. Growth increases the drift velocity, thereby reducing the effect of the outwarddiffusion and recondensation of the silicate component. Consequently, coagulation among silicates would bring the manyseeds model closer to the singleseed model due to a decrease in the enhancement of “locked” silicates outside the snowline. A similar trend is expected when the silicates that are released upon evaporation are larger. According to the experimental work of Aumatell & Wurm (2011), an icy aggregate of 1 cm in size breaks up into about 200 subaggregates when it evaporates. In any case, we expect that a more realistic “breakup” or coagulation model will lead to results that lie in between the results for our manyseeds and singleseed model designs.
In our work, we have also neglected coagulation among pebbles. On the one hand, one could think that icy pebbles on their way to the snowline would grow even more because of coagulation – at least as long their relative velocities stay low enough. On the other hand, according to Sirono (2011) and Okuzumi et al. (2016), the fragmentation threshold velocity for icy pebbles near the snowline is reduced due to sintering. This might motivate a smaller average icy pebble size (a lower τ_{3} in our nomenclature) and therefore a smaller radial drift velocity, which would further increase the solid surface density exterior to the snowline (see Fig. 9).
6.5. Observational implications
We showed that intermediatetohigh αvalues are most favorable for triggering streaming instability near the snowline. The onset of streaming instability manifests itself through the formation of a peak in the solidstogas ratio that grows in height (increasing Σ_{ice}) but also in width – the latter because collective effects cause pebbles to move slower. Even though more solids are required for high α and high Ṁ_{gas} than for low α and low Ṁ_{gas}, tens of Earth masses are sufficient to form the ice peak. This also means that tens of Earth masses can be stored in an annulus outside the snowline, especially when the system is characterized by high pebble and gas accretion rates. Such annuli of solid enhancement can be observable with facilities as ALMA. In the context of the snowline, the ring structure seen in the TW Hya system with a width of about 1 au (Andrews et al. 2016) might very well correspond to a realisation of the waterdiffusion effect in a highly turbulent disk with a high gas accretion rate.
The fact that the planets in the inner solar system are waterpoor (Marty 2012; McCubbin et al. 2012), even though the snowline should have migrated to 1 au before the disk was depleted, was pointed out as the “snowline problem” by Oka et al. (2011). The early formation of a protoplanet near the snowline might provide a solution to this problem, as proposed recently by Morbidelli et al. (2016). Once a protoplanet near the snowline has formed it could halt the inwarddrifting pebble flux, either by accreting the pebbles (Guillot et al. 2014), or by trapping them in pressure maxima created by the newborn planet (Zhu et al. 2014; Lambrechts et al. 2014). In the meantime, the water vapor gets accreted to the star and the snowline location migrates inward (e.g., Oka et al. 2011). Consequently, an early formation of a protoplanet near the snowline might explain the lack of water in the inner solar system. The water diffusion/condensation effect discussed in this paper provides a way to form planetesimals near the snowline in an early stage of the disk (i.e., when the snowline is still located outside of the current waterpoor region of the solar system). After planetesimals of a certain size have formed, they can subsequently accrete pebbles and quickly grow to larger bodies (e.g., Ormel & Klahr 2010; Lambrechts & Johansen 2012, 2014; Bitsch et al. 2015; Visser & Ormel 2016). Therefore, our water diffusion/condensation model provides the first key step to realize the early formation of a protoplanet near the snowline.
7. Conclusions
Our main findings can be summarized as follows.

1.
Water diffusion and condensation near the snowline can resultin an enhancement of a factor several in the ice surface density.Because of the dynamic setup of our model where water vapor iscarried away with the accreting gas, this enhancement is muchless than found by Stevenson & Lunine (1988).Nevertheless, the boost in the solidstogas ratio can still triggerstreaming instability, provided a large enough pebble flux.

2.
The peak in the ice surface density is not located at the snowline, but exterior to it (r_{peak}>r_{snow}). With larger incoming pebble flux, the peak becomes broader, because the backreaction of the solids on the gas reduces the pebble drift velocity. Depending on the turbulence strength, the width of the peak can be as much as ~1 au.

3.
Such broad peaks can contain tens of Earth masses in pebbles, appearing as bright annuli at radio wavelengths.

4.
The release of many micronsized silicate grains upon evaporation of icy pebbles produces a peak in “locked” silicates exterior to the snowline, due to diffusion and sweepup of the silicates. This peak adds to the ice peak and therefore enforces the enhancement of the solidstogas ratio outside the snowline.

5.
Interior to the snowline, the solidstogas ratio is boosted if many micronsized silicate grains are released during evaporation, because they cause a “traffic jam” effect. However, because silicate grains mix with the background gas before they cross the snowline, the solidstogas ratio enhancement just interior to r_{snow} is limited.

6.
In the context of a viscous disk model, the ratio between the accretion rate of solids and gas needs to be of order ~0.1 in order to reach solidstogas midplane ratios of the order of tens percent. The mechanism operates best at intermediate (~10^{3}) αvalues. Therefore, planetesimals can form at an early time in the evolution of the disk.
Dra¸żkowska et al. (2016) argue that growth and radial drift can lead to pileups in the inner disk, where streaming instability may then be triggered. Recently, Gonzalez et al. (2017) also presented a pileup mechanism.
For simplicity, we have ignored other contributions to Δv_{sil,peb}. Turbulent velocities, however, may dominate over radial drift motion when α is large (Cuzzi & Hogan 2003; Ormel & Cuzzi 2007). Accounting for turbulent relative velocities will result in an increase of the peak solidstogas ratio of ~10% (e.g., 20% for our fiducial parameters presented in Table 1).
We stress again that the model assumes that the incoming pebble mass flux is constant over time (see Sect. 4.1). However, the amount of solids needed to form the peak is independent of this assumption.
Acknowledgments
D.S. and C.W.O. are supported by the Netherlands Organization for Scientific Research (NWO; VIDI project 639.042.422). We would like to thank Jonathan Guyer and Daniel Wheeler for their elaborate answers to FiPyrelated questions. We would also like to thank Carsten Dominik, Shigeru Ida, Satoshi Okuzumi, Anders Johansen, Daniel Carrera and the other participants of the Lorentz workshop “New directions in Planet Formation” (Leiden, July 2016) for stimulating discussions. We are indebted to Sebastiaan Krijt, Jeff Cuzzi, and the anonymous referee for constructive feedback on the manuscript.
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Appendix A: List of symbols
A list of frequentlyused symbols is given in Table A.1.
Frequentlyused symbols.
Appendix B: Expression collective effects
Expressions for the aerodynamic drift of single particles have been derived by Whipple (1972) and Weidenschilling (1977) for nonaccreting disks. Later, Nakagawa et al. (1986) accounted for the backreaction forces that the particles collectively exert on the gas. The gas motion is then outwards while the total dust+gas mass flux becomes zero. These expressions can be generalized to account for a size distribution of particles (Tanaka et al. 2005; Estrada & Cuzzi 2008; Bai & Stone 2010).
In (steady) accretion disks gas moves inwards at a rate that is set by the viscosity. This modifies the single particle drift expressions. In particular, small particles, which show negligible radial drift, nevertheless move inwards as they are carried by the gas. While for the single particle case the modification of the drift expressions for accreting disks is straightforward, expressions accounting for both collective effects and viscosity have, to the best of our knowledge, not yet been presented. We derive those here.
The equations of motions in a frame corotating with the local Keplerian period read: where v is the particle velocity and u the gas velocity, D / Dt is the material derivative, the first term on the RHS is the drag force, the second term is the Coriolis force, and F_{Euler} = − (dΩ_{K}/ dt) × r is the Euler force that arises due to the radial motion. It therefore appears in the radial equations. In addition, the equation of motion for the gas includes a hydrostatic correction due to a radial pressure gradient (F_{∇P}) and viscous forces (F_{ν}). Following convention, we write the pressure gradient in terms of a nondimensional η: (B.2)and use the thin disk approximation (consider column densities Σ_{gas} instead of ρ) for the viscous force: (B.3)where T is the viscous stress tensor. In cylindrical coordinates, the only relevant term is: (B.4)with which the viscous force becomes (B.5)where ν is the kinematic viscosity. In the αdisk model we have that νΣ_{gas} is constant and therefore (B.6)In order to solve for the drift velocities, we put the accelerations on the LHS of Eq. (B.1) zero, Du/ Dt = Dv/ Dt = 0. This is justified, because a change in the drift velocities occurs on a timescale of ~r/v_{r}, which is always much longer than the stopping time. Inserting Eqs. (B.2) and (B.6) into (B.1) gives a system of four equations and four unknowns (the velocities). Its solution is: (B.7)where τ_{s} = t_{stop}Ω_{K}, ξ = ρ_{d}/ρ_{g}, and . Note that in the αprescription , that is, for α ≪ 1 the modification due to viscosity is minor.
Appendix C: Semianalytical model
In this section we aim for an analytic prescription of the key characteristics of the steadystate ice and vapor distribution for any given disc model – not necessarily with the same gas and temperature profiles as assumed in this study. We will derive expressions for the peak of the ice surface density and its location, which enable us to determine whether the conditions for streaming instability beyond the snowline can be reached.
Appendix C.1: Location of the snowline
The location of the snowline, r_{snow}, is the outermost radius where the entire incoming ice flux can thermodynamically exist in the gaseous state. Its location is found by equating the equilibrium (saturation) pressure to the vapor pressure of H_{2}O corresponding to the incoming icy pebble flux, that is, P_{eq} = P_{Z,a}, where P_{Z,a} is the steadystate vapor pressure; i.e., the vapor pressure obtained when all the H_{2}O is in the gas phase. Therefore, the snowline r_{snow} is given by the radius r where (C.1)see Eqs. (11) and (34). Given Ṁ_{ice}, α and a disk model, we can therefore readily solve (numerically) for r_{snow}.
A caveat of Eq. (C.1) is that the role of transport processes are neglected. These could potentially introduce disequilibrium corrections. However, we find that the times to achieve the equilibrium (saturation) pressure is typically much shorter than the transport timescales (by diffusion or drift).
Appendix C.2: The equilibrium density
Generalizing the above arguments to locations beyond r_{snow}, we approximate the vapor pressure with the saturation pressure – an approximation that is again justified as long as the timescales for evaporation (and condensation) are sufficiently short (in other words: the supersaturation level is small). Similarly, we can define a vapor surface density (Σ_{eq}) corresponding to P_{eq}. Rearranging Eq. (C.1) in terms of Σ we obtain this equilibrium surface density: (C.2)where Σ_{snow} and T_{snow} are the vapor surface density and the temperature at the location of the snowline. In Eq. (C.2) we have assumed powerlaws for the temperature, gas surface density, and the gas scaleheight. In our case we have p = 7 / 4 and q = 1 / 2 (see Sect. 2.1).
Taylorexpanding the (weaklyvarying) powerlaws involved in the expression of Σ_{eq} around r_{snow} gives^{7}: (C.3)where x = (r − r_{snow}) /r_{snow} is the fractional distance beyond the snowline and (C.4)is a dimensionless number that weakly depends on the location of the snowline.
Fig. C.1
Vapor surface density profiles. Shown in black are the steady state vapor profile when all the ice is in the gas phase (thin solid curve), and the surface density corresponding to equilibrium vapor pressure P_{eq} (Eq. (C.2); dashed solid curve). The snowline r_{snow} is located at the intersection of these two curves. The numericallyobtained profile (thick gray curve) closely follows the minimum of steadystate and equilibrium profiles. The blue curves present mathematicallyconvenient approximations to Σ_{eq} (see text), valid for r>r_{snow}. 
In Fig. C.1 the respective vapor density profiles have been plotted. Parameters correspond to those of the default model (Table 1). The simulated result of Sect. 4 is plotted by the thick gray curve. It is characterized by a sharp dent at r_{snow}. Exterior to the snowline Σ_{Z} follows the equilibrium profile (solid black curve), while interior to r_{snow}, it is limited by the imposed mass flux (solid dashed curve). The approximate expressions derived in Eq. (C.3), valid for r>r_{snow}, are shown by the blue curves. We obtain r_{snow} = 2.09 au, Σ_{snow} = 92 g cm^{2} and a_{eq} = 16.9. The solid blue curve approximates Σ_{eq} very closely. The dashed blue curves gives a further approximation to Σ_{eq}, obtained by putting p = 0. This slightly underestimates Σ_{Z} but nevertheless gives a reasonable approximation that we will use below.
Assuming Σ_{Z} = Σ_{eq} for the vapor density beyond r_{snow}, we write for the associated mass flux ℳ_{Z}:(C.5)where we neglected the curvature of the disk, i.e., we assumed that the scales over which Σ_{eq} and Σ_{gas} change are much smaller than r. This is justified as long as x ≪ 1. In a similar vein, we assume that quantites as D_{gas} and v_{gas} do not vary. With Eq. (C.3) for Σ_{eq} we obtain: where b_{gas} = v_{gas}r_{snow}/D_{gas} is the dimensionless gas velocity and in the last step p = 0. In a viscouslyevolving disk v_{gas} = 3ν/ 2r and hence b_{gas} = 1.5.
Appendix C.3: The ice profile
With the equilibrium profile as the approximation to the vapor density, we solve for the surface density of the ice by invoking conservation of mass. In steadystate the total H_{2}O mass flux ℳ_{tot,ice} = ℳ_{ice} + ℳ_{Z} is constant. Interior to the snowline, ℳ_{Z} = ℳ_{tot,ice} while for r ≫ r_{snow}ℳ_{Z} ≪ ℳ_{ice} ≈ ℳ_{tot,ice}. But near the snowline the mass fluxes change rapidly. Here, the steep gradient in the vapor density causes an outward (positive) mass flux, which increases the inwardlydirected icy pebble flux: (C.8)(Note that just outside r_{snow}, ℳ_{ice} and ℳ_{tot,ice} are negative and ℳ_{Z} is positive.) With ℳ_{eq} for ℳ_{Z} Eq. (C.8), in terms of x, reads (C.9)where b_{peb} = r_{snow}v_{peb}/D_{p} is the ratio between the speed at which the pebbles drift in and the radial velocity of the gas. Usually, pebbles outpace the gas and b_{peb} ≫ 1.
To solve Eq. (C.9) we will assume that b_{peb} and other parameters are constant in x. Assuming constant b_{peb} is clearly an approximation, since the pebbles may (i) acquire thick icy mantles on their approach to the snowline but (ii) lose all their ice once their are very close to r_{snow}. Hence, the aerodynamical properties of the pebbles and therefore v_{peb} are expected to vary considerably. Disregarding these concerns, momentarily, the solution to Eq. (C.9) reads: (C.10)where we used Eq. (C.6) for ℳ_{eq}, put p = 0^{8} and defined ε = b_{peb}/a_{eq}, ε_{gas} = b_{gas}/a_{eq} and c_{ℳ} = − ℳ_{tot,ice}r_{snow}/ Σ_{snow}D_{p}(a_{eq} − b_{gas}) to keep the notation concise. Typically, ε_{gas} ≈ 1.5 /a_{eq} and c_{ℳ} are small numbers. In a steadystate viscous disk Σ_{snow} ≈ Ṁ_{ice}/ 2πrv_{gas} and ℳ_{tot,ice} = − Ṁ_{ice}/ 2πr_{snow}. Hence in a viscous disk c_{ℳ} is related to ε_{gas}: (C.11)In Fig. C.2 we plot Σ_{ice} for the parameters of the default model (Table 1). The simulated data are given by the thick grey curve while the analytical profiles are in blue – the more precise approximation (with p = 7 / 4; solid) and the p = 0 case in dashed. The analytical profiles fit the simulation data very well. The key parameter for the analytical profiles is the velocity of the pebbles v_{peb}. Here, we have chosen v_{peb} to be the pebble velocity at the ice peak r_{peak}, v_{peb} ≈ 2.4 m s^{1}, which provides a decent fit. The fit is somewhat sensitive to the choice of v_{peb}; for example, adopting v_{peb}(r_{peak}) with the initial value for m_{ice} (i.e., without deposition of vapor) would overestimate the numerical curve by 20%.
Fig. C.2
Steady state surface density of ice for the default model parameters. The simulated profile from the numerical model (thick grey line) is well reproduced by the full analytical solution using p = 7 / 4 (solid curve; formula not shown in the main text) and the further p = 0 approximation (dashed curve; Eq. (C.10)). The black square denotes the values corresponding to the mass peak (r_{peak},Σ_{peak}) given by Eqs. (C.12) and (C.13). 
Appendix C.4: Peak values and final tuning
Equation (C.10) has a maximum at (x,Σ_{ice}) = (x_{peak},Σ_{peak}) where (C.12)or r_{peak} = (1 + x_{peak})r_{snow} in dimensional units, and (C.13)Since c_{ℳ} and ε_{gas} are fixed, the latter expression only depends on ε. Lower ε – meaning: a smaller pebble velocity at r_{peak} – increases both the width (x_{peak}) and the magnitude of the ice peak, resulting in a more pronounced, “fatter” ice bump.
All that remains is to find an expression for the pebble velocity at the ice peak v_{peb}, which in turn depends on the amount of ice those pebbles have accreted. To obtain m_{peb} = m_{core} + m_{ice} we invoke conservation of the pebble number flux (C.14)Hence, we can obtain m_{ice} from Σ_{peak}, calculate the aerodynamical properties of the pebbles at the peak (i.e., their stopping time) and obtain the pebble velocity v_{peb}.
With Eq. (C.14) we have a closed system of expressions to obtain the relevant quantities at the ice peak. These can best be computed by an iterative scheme, e.g.,

1.
From (an initial guess for) ε obtain Σ_{peak} and the position of the ice peak r_{peak} from the ice flux conservation model, Eq. (C.13) .

From Σ_{peak}, obtain the ice mass m_{ice} at the ice peak from the pebble conservation law, Eq. (C.14).

3.
From m_{ice} and the gas properties at r = r_{peak}, compute the stopping time of the pebbles at r_{peak}. Update the pebble velocity v_{peb} and its normalized variant ε.
This scheme can easily be extended with collective and mean molecular weight effects (i.e., the complete model). Finally, in order to obtain a better match to our numerical results we adopt two adhoc empirical “fixes”. First we reduce Eq. (C.13) by 10%, which accounts for the fact that the p = 0 approximation tends to overestimate the peak. Secondly, we slightly increase ε when it drops below unity. This fix approximately accounts for curvature effects (not included in the model) that become apparent when the ice peak becomes broad (at low ε). Hence we take ε = max(ε ∗ ,ε ∗ ^{0.8}) where ϵ ∗ = (v_{peb,peak}r_{peak}/a_{2}D_{peak}) is the uncorrected value.
In Table C.1 a comparison of the model with the numericallyobtained peak parameters is given for a number of model parameters. Generally, the agreement is very good; the error in Σ_{peak} is at most 20%. Given its crudeness, the analytical model, however, does not always produce a perfect match – especially not when it comes to the profile. For example the low turbulence runs (α = 3 × 10^{4}), which imply high gas densities when Ṁ_{gas} is kept the same, still show a good match to Σ_{peak}, but the profile corresponding to Eq. (C.10) is very different from the numerical model. The reason for this is that pebbles enter the Stokes drag regime when approaching the ice peak, causing a sharp increase in the stopping time (and ε). The stopping time at the ice peak is in that case not representative for other radii.
Comparison between analytical and numerical model.
All Tables
All Figures
Fig. 1
Schematic showing the difference between the singleseed model and the manyseeds model for the internal structure of icy pebbles in the outer disk. In the singleseed model, the water ice layer (white) on the silicate core (red) becomes smaller at the evaporation front, and after complete evaporation of the ice, only one single silicate core remains. Since we take ζ = 0.5, the silicate core contains half the mass of the original pebble: m_{core} = m_{ice} = 0.5m_{p,start}. In the manyseeds model, pebbles in the outer disk consist of many micronsized silicate grains (red) “glued” together by water ice (white). As the ice evaporates, silicate grains are released as well. After complete evaporation of the ice, many micronsized silicate grains remain. Again, with ζ = 0.5, the total mass in silicate grains in a pebble in the outer disk is half of the total pebble mass, but this mass is now divided among many silicate grains that each have mass m_{sil}. See text for more details. 

In the text 
Fig. 2
The solution to the transport equations at different points in time, for the fiducial model parameters listed in Table 1. At t = 10^{5}yr, approximately 90% of the steadystate peak in the ice surface density has formed. a) Surface densities Σ of ice (solid lines) and vapor (dashed lines). The dotted line corresponds to the steadystate advectiononly vapor surface density profile. b) Midplane pebblestogas ratio ρ_{peb}/ρ_{gas}. c) Typical pebble mass m_{p}. d) Typical pebble internal density ρ_{•,p}. 

In the text 
Fig. 3
Rate of change of the ice surface density at the peak location, as function of time. The rate of change increases until the icy pebble front has reached the peak location, after which the peak continues to grow at an exponentially decreasing rate, while the system is converging to its steadystate solution. 

In the text 
Fig. 4
Steadystate results for the fiducial parameters, for the simple model with singleseed evaporation (upper two panels) and manyseeds evaporation (lower two panels). a) Surface densities of ice, silicates and vapor (Σ_{ice}, Σ_{sil}, and Σ_{Z}, respectively) for the singleseed model. The silicates are locked in the icy pebbles outside the snowline, whereas they are bare grains interior to the snowline. b) Midplane pebblestogas ratio ρ_{peb}/ρ_{gas}, and pebblestogas column density ratio Σ_{peb}/ Σ_{gas} for the singleseed model. c) Same as panel a) but for the manyseeds model. The silicates are now divided in two populations: silicates that are locked up in icy pebbles (Σ_{dirt}), and free silicates (Σ_{sil}). Note that in panels a) and c) the xaxis ranges between r = 1.8 − 2.8au, for clarity. d) Same as b), but for the manyseeds model and with an additional line for the midplane “free silicates”togas ratio ρ_{sil}/ρ_{gas}. 

In the text 
Fig. 5
Comparison of steadystate results for the fiducial parameters between the simple model (dashed lines) and the complete model (solid lines), which includes collective effects and the effects of the variation of the mean molecular weight μ. The upper two panels correspond to the singleseed evaporation model; the lower two panels correspond to the manyseeds evaporation model. In the latter case, we made the conservative choice of not including the free silicates in the backreaction onto the gas. a) Surface densities of ice (Σ_{ice}), vapor (Σ_{Z}) and silicates (Σ_{sil}) for the singleseed model. The grey line indicates the mean molecular weight of the gas in units of proton mass m_{H}. b) Midplane pebblestogas ratio ρ_{peb}/ρ_{gas}. c) Same as a), but the silicates are now divided into “free silicates” (Σ_{sil}) and “locked silicates” (Σ_{dirt}). For clarity, we only show the clean Σ_{ice} profile for comparison. d) Same as b), with an additional line denoting the “free silicates”togas ratio ρ_{sil}/ρ_{gas}. 

In the text 
Fig. 6
Comparison of steadystate results for the simple, singleseed, fiducial model between the case where vapor has the same vertical distribution as the background gas (H_{Z} = H_{gas}) and the case where vapor has the same scale height as the pebbles (H_{Z} = H_{peb}). In all three panels, solid lines correspond to the H_{Z} = H_{gas} case and dashed lines correspond to the H_{Z} = H_{peb} case. a) Steadystate water ice (blue) and water vapor (green) surface densities. b) Midplane solidstogas ratios (green) and solidstogas surface densities ratios (blue). c) Typical pebble mass m_{p}. 

In the text 
Fig. 7
a) Contours of constant relative ice surface density peak heights f_{Σ,peak} (see text for details) as function of turbulence parameter α and solidstogas accretion rate ℱ_{s / g}. The gas accretion rate Ṁ_{gas} is fixed to 10^{8}M_{⊙}yr^{1} and the initial size of the pebbles τ_{3} is fixed to 0.03. b) Contours of constant relative ice surface density peak heights (see text for details) as function of the turbulence parameter α and the gas accretion rate Ṁ_{gas}. The solidstogas accretion rate ratio ℱ_{s / g} is fixed to 0.4 and the initial size of the pebbles τ_{3} is fixed to 0.03. The cyan lines denote a Toomre parameter (Q_{T}) of unity at 10 au (1 au); the space below these lines has Q_{T}< 1 and is gravitationally unstable at 10 au (1 au). 

In the text 
Fig. 8
a) Contours of midplane solidstogas ratios (black) as function of the turbulence parameter α and the solidstogas accretion rate ℱ_{s / g}. The gas accretion rate Ṁ_{gas} is fixed to 10^{8}M_{⊙}yr^{1} and the initial size of the pebbles τ_{3} is fixed to 0.03. Orange contours denote the amount of solid material (in Earth masses) that is required to form the eventual peak in the ice surface density just outside the snowline. b) Contours of midplane solidstogas ratios as function of α and Ṁ_{gas}. The solidstogas accretion rate ℱ_{s / g} is fixed to 0.4 and the initial size of the pebbles τ_{3} is fixed to 0.03. Orange contours denote the amount of solid material (in Earth masses) that is required to form the eventual peak in the ice surface density just outside the snowline. The cyan lines denote a Toomre parameter (Q_{T}) of unity at 10 au (1 au); the space below these lines has Q_{T}< 1 and is gravitationally unstable at 10 au (1 au). 

In the text 
Fig. 9
Peak midplane solidstogas ratio as function of τ_{3}. Ṁ_{gas} is fixed at 10^{8}M_{⊙}yr^{1}, ℱ_{s / g} at 0.4, and the value of α is 3 × 10^{3}. We can distinguish four regimes I–IV, which are explained in the main text. 

In the text 
Fig. C.1
Vapor surface density profiles. Shown in black are the steady state vapor profile when all the ice is in the gas phase (thin solid curve), and the surface density corresponding to equilibrium vapor pressure P_{eq} (Eq. (C.2); dashed solid curve). The snowline r_{snow} is located at the intersection of these two curves. The numericallyobtained profile (thick gray curve) closely follows the minimum of steadystate and equilibrium profiles. The blue curves present mathematicallyconvenient approximations to Σ_{eq} (see text), valid for r>r_{snow}. 

In the text 
Fig. C.2
Steady state surface density of ice for the default model parameters. The simulated profile from the numerical model (thick grey line) is well reproduced by the full analytical solution using p = 7 / 4 (solid curve; formula not shown in the main text) and the further p = 0 approximation (dashed curve; Eq. (C.10)). The black square denotes the values corresponding to the mass peak (r_{peak},Σ_{peak}) given by Eqs. (C.12) and (C.13). 

In the text 
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