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 As a major objective of the project, we successfully collected novel high-quality radar datasets, where triple-frequency Doppler spectra are combined with spectral W-Band polarimetry covering a large variety of winter clouds. The first of the two proposed campaigns (second campaign was delayed due to COVID-19 and is currently planned for winter 2021/22) was successfully carried out from Nov. 2018 until Jan. 2019 at the Jülich ObservatorY forCloud Evolution Core Facility (JOYCE-CF, Löhnert et al. (2015); see also Fig. 1). The quality-controlled and post-processed dataset allowed to develop new approaches for radar calibration using polarimetric Doppler spectra (Myagkov et al., 2020) and for estimating total path attenuation and multi-frequency relative calibration (Tridon et al., 2020). A new triple-frequency retrieval of the rain PSD (Mróz et al., 2020) has been developed, which also allowed to better understand the link between rainfall and snow properties aloft (Mróz et al., 2021).\\ As a major objective of the project, we successfully collected novel high-quality radar datasets, where triple-frequency Doppler spectra are combined with spectral W-Band polarimetry covering a large variety of winter clouds. The first of the two proposed campaigns (second campaign was delayed due to COVID-19 and is currently planned for winter 2021/22) was successfully carried out from Nov. 2018 until Jan. 2019 at the Jülich ObservatorY forCloud Evolution Core Facility (JOYCE-CF, Löhnert et al. (2015); see also Fig. 1). The quality-controlled and post-processed dataset allowed to develop new approaches for radar calibration using polarimetric Doppler spectra (Myagkov et al., 2020) and for estimating total path attenuation and multi-frequency relative calibration (Tridon et al., 2020). A new triple-frequency retrieval of the rain PSD (Mróz et al., 2020) has been developed, which also allowed to better understand the link between rainfall and snow properties aloft (Mróz et al., 2021).\\
  
-An impression of the rich information content of the new combined dataset is given in Fig. 1 which is also discussed in more detail in Trömel et al., 2021. The KDP indicates a steep increase in ice particle concentration below the -15°C temperature level which continues down to the surface (note that KDP at W-band is 10 times more sensitive than at X-band). The strongest KDP also coincides with the detection of largest aggregate sizes in the dual-wavelength ratio (DWR). Particularly enlightening is the analysis of those observables as Doppler spectra, where a distinction to particles with different terminal velocities (often proportional to their size) can be obtained (Fig. 1d-e). We find that medium-sized aggregates fall from above and once reaching the -15°C level, a secondary, slow mode appears in the spectrum whose very large spectral ZDR values indicate that this mode is composed of plate-like crystals. Currently, we derive statistics of this feature including newly derived radar variables, such as the spectral edge velocity, to better understand which role for example secondary ice processes might play in explaining the observed signatures. For this analysis, we also profit from high-resolution (600m hor. res.) ICON-LEM simulations, which are available at UoC for the entire campaign. Improving the simulation of ice and snow particles (Karrer et al., 2020) and their scattering properties (Ori et al., 2021) enabled us to further develop our radar forward operator, which is the basis for model-observation statistics such as done for non-polarimetric multi-frequency data in Ori et al., 2020. For specific case studies, the new 1D Lagrangian super-particle model McSnow (Brdar and Seifert, 2018) is run in close collaboration with DWD, which has been extended within IMPRINT by a habit prediction scheme and parametrizations of secondary ice processes. +An impression of the rich information content of the new combined dataset is given in Fig. 1 which is also discussed in more detail in Trömel et al., 2021. The $K_\mathrm{DP}$ indicates a steep increase in ice particle concentration below the $-15^\circ\mathrm{C}$ temperature level which continues down to the surface (note that $K_\mathrm{DP}$ at W-band is 10 times more sensitive than at X-band). The strongest $K_\mathrm{DP}$ also coincides with the detection of largest aggregate sizes in the dual-wavelength ratio ($\mathrm{DWR}$). Particularly enlightening is the analysis of those observables as Doppler spectra, where a distinction to particles with different terminal velocities (often proportional to their size) can be obtained (Fig. 1d-e). We find that medium-sized aggregates fall from above and once reaching the $-15^\circ\mathrm{C}$ level, a secondary, slow mode appears in the spectrum whose very large spectral $Z_\mathrm{DR}$ values indicate that this mode is composed of plate-like crystals. Currently, we derive statistics of this feature including newly derived radar variables, such as the spectral edge velocity, to better understand which role for example secondary ice processes might play in explaining the observed signatures. For this analysis, we also profit from high-resolution ($600\,\mathrm{m}$ hor. res.) ICON-LEM simulations, which are available at UoC for the entire campaign. Improving the simulation of ice and snow particles (Karrer et al., 2020) and their scattering properties (Ori et al., 2021) enabled us to further develop our radar forward operator, which is the basis for model-observation statistics such as done for non-polarimetric multi-frequency data in Ori et al., 2020. For specific case studies, the new 1D Lagrangian super-particle model McSnow (Brdar and Seifert, 2018) is run in close collaboration with DWD, which has been extended within IMPRINT by a habit prediction scheme and parametrizations of secondary ice processes. 
-\\ + 
-\\ +<met figure 
-{{ fiqure_1_imprint_2021.png?direct&650 }} \\ +    src="https://www2.meteo.uni-bonn.de/spp2115/lib/exe/fetch.php?media=projects:fiqure_1_imprint_2021.png" 
-<WRAP tablewidth 60% center>**Figure 1:** Combined triple-frequency and W-band polarimetric observations from a snowfall event observed on 22th Jan. 2019 at the JOYCE-CF site in Jülich, Germany: a) Dual-wavelength ratio (DWR) between Ka and W-band, b) differential reflectivity (ZDR) and c) specific differential phase (KDP) from the polarimetric W-band radar. Vertical profiles of  Doppler spectra of DWR (d) and ZDR (e) and KDP (f) are shown as a function of in-cloud temperature. The time from which the spectra are taken is indicated by the vertical red dashed line in a)-c). Note that the polarimetric data have been observed at a constant elevation angle of 30°; all profiles have been projected to zenith to allow an easier comparison with the zenith observations of the three other radars (Figure from Trömel et al., 2021).</WRAP> +    width="900" 
-\\ +    fit="responsive" 
-\\+    title="Figure 1" 
 +    caption="Combined triple-frequency and W-band polarimetric observations from a snowfall event observed on 22th Jan. 2019 at the JOYCE-CF site in Jülich, Germany: a) Dual-wavelength ratio ($\mathrm{DWR}$) between Ka and W-band, b) differential reflectivity ($Z_\mathrm{DR}$) and c) specific differential phase ($K_\mathrm{DP}$) from the polarimetric W-band radar. Vertical profiles of Doppler spectra of $\mathrm{DWR}$ (d) and $Z_\mathrm{DR}$ (e) and $K_\mathrm{DP}$ (f) are shown as a function of in-cloud temperature. The time from which the spectra are taken is indicated by the vertical red dashed line in a)-c). Note that the polarimetric data have been observed at a constant elevation angle of $30^\circ$; all profiles have been projected to zenith to allow an easier comparison with the zenith observations of the three other radars (Figure from Trömel et al., 2021)." 
 +    caption-align="left" 
 +    load-animation="zoom-in" 
 +    zoomable lightbox> 
 **Contribution of Deutscher Wetterdienst (DWD)**\\ **Contribution of Deutscher Wetterdienst (DWD)**\\
  
 At DWD the main focus is to improve cloud and precipitation schemes in atmospheric models based on process fingerprints detectable in polarimetric observations. While bulk microphysical schemes often lack details because of generalizations, Monte-Carlo Lagrangian particle models (LPMs) allow avoiding intrinsic errors caused by such assumptions. The DWD-developed LPM McSnow (Brdar and Seifert, 2018) allows the straightforward implementation of the current knowledge about microphysical processes and provides a way to track the growth history of particles. \\ At DWD the main focus is to improve cloud and precipitation schemes in atmospheric models based on process fingerprints detectable in polarimetric observations. While bulk microphysical schemes often lack details because of generalizations, Monte-Carlo Lagrangian particle models (LPMs) allow avoiding intrinsic errors caused by such assumptions. The DWD-developed LPM McSnow (Brdar and Seifert, 2018) allows the straightforward implementation of the current knowledge about microphysical processes and provides a way to track the growth history of particles. \\
 We extended McSnow to allow the natural development of ice habits by depositional growth and riming to eliminate mass to diameter relationships (at least for primary ice particles) and constrain the behavior by comparing the resulting particle shape to the large polarimetric signal typically caused by the asymmetry of ice crystals. Since the manifoldness of ice crystal shapes is sheer endless, we assume them to be oblate or prolate spheroids. Figure 2 shows the influence of the ice habit on the particle’s ice mass after 10 minutes of depositional growth at constant temperature and water saturation. The comparison with wind tunnel measurements (blue open squares, Takahashi et al. 1991) makes it apparent that the assumption of a spherical particle can greatly underestimate ice masses and illustrates the need for an explicit habit consideration to capture the temperature-dependent growth regimes. We extended McSnow to allow the natural development of ice habits by depositional growth and riming to eliminate mass to diameter relationships (at least for primary ice particles) and constrain the behavior by comparing the resulting particle shape to the large polarimetric signal typically caused by the asymmetry of ice crystals. Since the manifoldness of ice crystal shapes is sheer endless, we assume them to be oblate or prolate spheroids. Figure 2 shows the influence of the ice habit on the particle’s ice mass after 10 minutes of depositional growth at constant temperature and water saturation. The comparison with wind tunnel measurements (blue open squares, Takahashi et al. 1991) makes it apparent that the assumption of a spherical particle can greatly underestimate ice masses and illustrates the need for an explicit habit consideration to capture the temperature-dependent growth regimes.
-\\ + 
-\\ +<met figure 
-{{ fiqure_2_imprint_2021.png?direct&650 }} \\ +    src="https://www2.meteo.uni-bonn.de/spp2115/lib/exe/fetch.php?media=projects:fiqure_2_imprint_2021.png" 
-<WRAP tablewidth 60% center>**Figure 2:** Temperature-dependent mass growth after 10 min of vapor deposition. The black line shows the results for a crystal that can grow asymmetrical, grey line for a spherical crystal. Blue open squares are measurements from Takahashi et al. (1991).</WRAP> +    width="650" 
-\\ +    fit="responsive" 
-\\ +    title="Figure 2" 
-The initial atmospheric conditions at nucleation showed to be of special importance for the further development of the particle since they crucially influence the particle’s shape and therefore mass and lifetime. Primary crystals that initially developed into a certain shape (pro- or oblate) tend to only rarely change their habit even in unfavorable atmospheric regimes. This effect results in a thermo- and hydrodynamical feedback that influence the mass and therefore the lifetime essentially.\\+    caption="Temperature-dependent mass growth after $10\,\mathrm{min}$ of vapor deposition. The black line shows the results for a crystal that can grow asymmetrical, grey line for a spherical crystal. Blue open squares are measurements from Takahashi et al. (1991)." 
 +    caption-align="left" 
 +    load-animation="zoom-in" 
 +    zoomable lightbox> 
 + 
 +The initial atmospheric conditions at nucleation showed to be of special importance for the further development of the particle since they crucially influence the particle’s shape and therefore mass and lifetime. Primary crystals that initially developed into a certain shape (pro- or oblate) tend to only rarely change their habit even in unfavorable atmospheric regimes. This effect results in a thermo- and hydrodynamical feedback that influence the mass and therefore the lifetime essentially. 
 The coupling of McSnow and ICON is a crucial tool we are working with that helps to estimate the impact of the ice habit as well as the collision fragmentation in 2D/3D simulations. To better understand the impact, a recent parameterization of ice particle collisional fragmentation (Phillips et al., 2017) has been implemented into McSnow, complementing already included secondary ice processes, such as rime splintering. Only in real case setups the full spectrum of hydro- and thermodynamical feedbacks is present and therefore unveils the full impact. The coupling of McSnow and ICON is a crucial tool we are working with that helps to estimate the impact of the ice habit as well as the collision fragmentation in 2D/3D simulations. To better understand the impact, a recent parameterization of ice particle collisional fragmentation (Phillips et al., 2017) has been implemented into McSnow, complementing already included secondary ice processes, such as rime splintering. Only in real case setups the full spectrum of hydro- and thermodynamical feedbacks is present and therefore unveils the full impact.
 \\ \\
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 **Collaborative work**\\ **Collaborative work**\\
  
-To compare the habit-affected simulations with observations, the results have to be transferred from model to observational space via a forward operator. An example of forward simulated radar polarimetric spectra and moments based on the new habit prediction implemented in McSnow is shown in Figure 3. Currently, those simulations are being refined and extended to better understand the origin and cause of observed aggregation signatures as presented for example in Figure 1. \\ +To compare the habit-affected simulations with observations, the results have to be transferred from model to observational space via a forward operator. An example of forward simulated radar polarimetric spectra and moments based on the new habit prediction implemented in McSnow is shown in Figure 3. Currently, those simulations are being refined and extended to better understand the origin and cause of observed aggregation signatures as presented for example in Figure 1. 
-{{ fiqure_3_imprint_2021.png?direct&750 }} \\+
  
-<WRAP tablewidth 60% center>**Figure 3:** Example 1D simulation with McSnow and the newly implemented habit prediction scheme: In a) one can see how the particle concentration of single crystals decreases due to aggregation. The model output was then used to simulate polarimetric moments and spectra: (b) KDP , (c) ZDR , and (d) Doppler spectra of ZDR.</WRAP>\\+<met figure 
 +    src="https://www2.meteo.uni-bonn.de/spp2115/lib/exe/fetch.php?media=projects:fiqure_3_imprint_2021.png" 
 +    width="650" 
 +    fit="responsive" 
 +    title="Figure 3" 
 +    caption="Example 1D simulation with McSnow and the newly implemented habit prediction scheme: In a) one can see how the particle concentration of single crystals decreases due to aggregation. The model output was then used to simulate polarimetric moments and spectra: (b) $K_\mathrm{DP}$, (c) $Z_\mathrm{DR}$, and (d) Doppler spectra of $Z_\mathrm{DR}$." 
 +    caption-align="left" 
 +    load-animation="zoom-in" 
 +    zoomable lightbox>
  
-In the last phase of IMPRINT, we now have all tools at hand to investigate specific microphysical processes by trying to reproduce common observational features, such as the rapid aggregation occurring at -15°C (see Fig. 1), with the new habit-dependent McSnow model. Our ongoing simulation studies strongly hint at secondary ice processes being highly relevant for explaining the observed radar signatures. In an upcoming cooperation with V. Phillips (Lund University) we plan to extend the parameterization for collisional fragmentation due to the addition of a dependency of the number of fragments released in every fragmentation on habits of the collision pair.+In the last phase of IMPRINT, we now have all tools at hand to investigate specific microphysical processes by trying to reproduce common observational features, such as the rapid aggregation occurring at $-15^\circ\mathrm{C}$ (see Fig. 1), with the new habit-dependent McSnow model. Our ongoing simulation studies strongly hint at secondary ice processes being highly relevant for explaining the observed radar signatures. In an upcoming cooperation with V. Phillips (Lund University) we plan to extend the parameterization for collisional fragmentation due to the addition of a dependency of the number of fragments released in every fragmentation on habits of the collision pair.
 \\ \\
 \\ \\
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 **Contribution of University of Cologne**\\ **Contribution of University of Cologne**\\
  
-The contribution from the University of Cologne focuses on multi-frequency spectral Radar +The contribution from the University of Cologne focuses on multi-frequency spectral Radar polarimetric Observations and the polarimetric 1D radar forward operator. The first of two proposed winter campaigns (TRIPEx-pol) took place in Jülich from 1st Nov. 2018 until 19th Feb. 2019. During the campaign, vertically pointing X-Band, Ka-Band and W-Band Doppler radars as well as a scanning polarimetric W-Band radar were installed at the Jülich ObservatorY for Cloud Evolution – Core Facility (JOYCE-CF) (see Figure 1).\\
-polarimetric Observations and the polarimetric 1D radar forward operator. The first of two +
-proposed winter campaigns (TRIPEx-pol) took place in Jülich from 1st Nov. 2018 until 19th +
-Feb. 2019. During the campaign, vertically pointing X-Band, Ka-Band and W-Band Doppler +
-radars as well as a scanning polarimetric W-Band radar were installed at the Jülich +
-ObservatorY for Cloud Evolution – Core Facility (JOYCE-CF) (see Figure 1).\\+
 \\ \\
-These measurements were complemented by the two polarimetric X-Band radars stationed in Bonn +These measurements were complemented by the two polarimetric X-Band radars stationed in Bonn and the Sophienhöhe and by 20 Radiosondes launched during the campaign. A first look at the dataset shows that the measurement setup is capable to capture ice microphysical processes: the polarimetric moment differential radar reflectivity $Z_\mathrm{DR}$ in Figure 2 shows aggregation at around 14–16 UTC below $3000\,\mathrm{m}$ (small values of $Z_\mathrm{DR}$), whereas the enhancement of the differential specific phase shift $K_\mathrm{DP}$ in the same period indicates the presence of small, asymmetric particles. The spectral $Z_\mathrm{DR}$ and spectral dual-wavelength ratio $\mathrm{DWR}_\mathrm{Ka,W}$ allow to look at the smaller particles present (to which the moments of $Z_\mathrm{DR}$ and $Z_\mathrm{e}$ are insensitive as soon as larger particles dominate the signal). Looking at Figure 3, the spectral $\mathrm{DWR}$s clearly indicate aggregation in the height region associated with temperatures between $-10$ and $-8^\circ\mathrm{C}$ . The Doppler spectra also show a widening just below $-16^\circ\mathrm{C}$, which might indicate secondary ice production at this height. Simultaneously, the spectral $Z_\mathrm{DR}$ shows a large amount of small particles appearing below $-16^\circ\mathrm{C}$, that can be consistently observed in the measurement volume down to the ground.\\
-and the Sophienhöhe and by 20 Radiosondes launched during the campaign. A first look at +
-the dataset shows that the measurement setup is capable to capture ice microphysical +
-processes: the polarimetric moment differential radar reflectivity ZDR in Figure 2 shows +
-aggregation at around 14-16 UTC below 3000m (small values of ZDR), whereas the +
-enhancement of the differential specific phase shift KDP in the same period indicates the +
-presence of small, asymmetric particles. The spectral ZDR and spectral dual-wavelength +
-ratio DWR Ka-W allow to look at the smaller particles present (to which the moments of ZDR +
-and Ze are insensitive as soon as larger particles dominate the signal). Looking at Figure 3, +
-the spectral DWRs clearly indicate aggregation in the height region associated with +
-temperatures between -10 and -8°C. The Doppler spectra also show a widening just below +
--16°C, which might indicate secondary ice production at this height. Simultaneously, the +
-spectral ZDR shows a large amount of small particles appearing below -16°C, that can be +
-consistently observed in the measurement volume down to the ground.\\ +
-\\ +
-In order to get the most information from the available dataset, it is currently reprocessed +
-and quality-controlled following the approach described in Dias Neto et al 2019. +
-Furthermore, nested, high-resolution ICON-LEM simulations have been conducted for the +
-entire campaign. The multifrequency radar moments forward modeled with Pamtra such as +
-the equivalent radar reflectivity factor Ze or the mean Doppler velocity show a good +
-agreement with the observations and provide a good starting point for analysing the ice +
-microphysics implemented in the model.\\ +
-\\ +
-{{ imprint_figur1.png?direct&850  }} +
-\\ +
-<WRAP tablewidth 60% center>**Figure 1:** measurement setup at JOYCE-CF during the TRIPEx-pol campaign.</WRAP>\\+
 \\ \\
 +In order to get the most information from the available dataset, it is currently reprocessed and quality-controlled following the approach described in Dias Neto et al 2019. Furthermore, nested, high-resolution ICON-LEM simulations have been conducted for the entire campaign. The multifrequency radar moments forward modeled with Pamtra such as the equivalent radar reflectivity factor $Z_\mathrm{e}$ or the mean Doppler velocity show a good agreement with the observations and provide a good starting point for analysing the ice microphysics implemented in the model.\\
  
-{{  imprint_figur2.1.png?direct&600  }} +<met figure 
-\\ +    src="https://www2.meteo.uni-bonn.de/spp2115/lib/exe/fetch.php?media=projects:imprint_figur1.png" 
-{{  imprint_figur2.2.png?direct&600  }} +    width="900" 
-\\ +    fit="responsive" 
-<WRAP tablewidth 60% center>**Figure 2:** Differential reflectivity ZDR (top panel) and differential specific phase shift KDP (bottom panel) at an elevation angle of 30° measured with the polarimetric W-band radar stationed at JOYCE-CF during the TRIPEx-pol campaign.</WRAP>\\ +    title="Figure 1" 
-\\ +    caption="Measurement setup at JOYCE-CF during the TRIPEx-pol campaign." 
-{{  imprint_figur3.png?direct&750  }} +    caption-align="left" 
-\\ +    load-animation="zoom-in" 
-<WRAP tablewidth 60% center>**Figure 3:** Spectral dual-wavelength ratio DWR Ka-W (left panel) and spectral ZDR (right panel). Negative Doppler velocities (DV) denote a downward motion of the observed particles.</WRAP>\\ +    background="white" 
-\\+    zoomable lightbox> 
 + 
 +<met figure-grid 
 +    images='[ 
 +        {"src":"https://www2.meteo.uni-bonn.de/spp2115/lib/exe/fetch.php?media=projects:imprint_figur2.1.png"}, 
 +        {"src":"https://www2.meteo.uni-bonn.de/spp2115/lib/exe/fetch.php?media=projects:imprint_figur2.2.png"} 
 +    ]' 
 +    width="900" 
 +    title="Figure 2" 
 +    caption="Differential reflectivity $Z_\mathrm{DR}$ (top panel) and differential specific phase shift $K_\mathrm{DP}$ (bottom panel) at an elevation angle of $30^\circ$ measured with the polarimetric W-band radar stationed at JOYCE-CF during the TRIPEx-pol campaign." 
 +    caption-align="left" 
 +    columns="1" 
 +    layout="column" 
 +    load-animation="zoom-in" 
 +    background="white" 
 +    zoomable lightbox> 
 + 
 +<met figure 
 +    src="https://www2.meteo.uni-bonn.de/spp2115/lib/exe/fetch.php?media=projects:imprint_figur3.png" 
 +    width="900" 
 +    fit="responsive" 
 +    title="Figure 3" 
 +    caption="Spectral dual-wavelength ratio $\mathrm{DWR}_\mathrm{Ka,W}$ (left panel) and spectral $Z_\mathrm{DR}$ (right panel). Negative Doppler velocities ($\mathrm{DV}$) denote a downward motion of the observed particles." 
 +    caption-align="left" 
 +    load-animation="zoom-in" 
 +    background="white" 
 +    zoomable lightbox>
  
 **Contribution of Deutscher Wetterdienst (DWD)**\\ **Contribution of Deutscher Wetterdienst (DWD)**\\
Line 240: Line 255:
 At DWD the main focus is to improve cloud and precipitation schemes in atmospheric models based on process fingerprints detectable in polarimetric observations. While bulk microphysical schemes often lack details because of generalizations, Monte-Carlo Lagrangian particle models (LPMs) allow avoiding intrinsic errors caused by such assumptions. The DWD-developed LPM McSnow (Brdar and Seifert, 2018) allows the straightforward implementation of the current knowledge about microphysical processes and provides a way to track the growth history of particles. One key assumption still exists in analytical or empirical mass to diameter relationships that try to generalize particle habits and therefore determine their sedimentation velocity.\\ At DWD the main focus is to improve cloud and precipitation schemes in atmospheric models based on process fingerprints detectable in polarimetric observations. While bulk microphysical schemes often lack details because of generalizations, Monte-Carlo Lagrangian particle models (LPMs) allow avoiding intrinsic errors caused by such assumptions. The DWD-developed LPM McSnow (Brdar and Seifert, 2018) allows the straightforward implementation of the current knowledge about microphysical processes and provides a way to track the growth history of particles. One key assumption still exists in analytical or empirical mass to diameter relationships that try to generalize particle habits and therefore determine their sedimentation velocity.\\
 \\ \\
-By extending McSnow to allow the natural development of ice habits by depositional growth and riming, we eliminate these relationships (at least for primary ice particles) and can constrain the behavior by comparing the particle shape to the large polarimetric signal typically caused by the asymmetry of ice crystals. Since the manifoldness of ice crystal shapes is sheer endless, we assume them to be oblate or prolate spheroids. Figure 4 shows the influence of the ice habit on the mass of a particle after 10 minutes of depositional growth at constant temperature and water saturation. The comparison with wind tunnel measurements makes it apparent that the assumption of a spherical particle greatly underestimates ice mass and illustrates the need for an explicit habit consideration to capture the temperature-dependent growth regimes.\\+By extending McSnow to allow the natural development of ice habits by depositional growth and riming, we eliminate these relationships (at least for primary ice particles) and can constrain the behavior by comparing the particle shape to the large polarimetric signal typically caused by the asymmetry of ice crystals. Since the manifoldness of ice crystal shapes is sheer endless, we assume them to be oblate or prolate spheroids. Figure 4 shows the influence of the ice habit on the mass of a particle after $10\,\mathrm{min}$ of depositional growth at constant temperature and water saturation. The comparison with wind tunnel measurements makes it apparent that the assumption of a spherical particle greatly underestimates ice mass and illustrates the need for an explicit habit consideration to capture the temperature-dependent growth regimes.\\
 \\ \\
-The initial conditions at nucleation are important for the development of the particle, since they crucially influence mass, shape, and lifetime. An example of the variability invoked by the ice habit is shown in Figure 5. Identical particles were nucleated every 5 meters in an idealized atmosphere. Depending on the conditions at nucleation, the individual lifetime differs strongly (first plot). The lifetime is determined by the particle shape (third plot; Φ < 1 plate-like, Φ > 1 column-like) which strongly influences ice mass and sedimentation velocity (second and fourth plot).\\+The initial conditions at nucleation are important for the development of the particle, since they crucially influence mass, shape, and lifetime. An example of the variability invoked by the ice habit is shown in Figure 5. Identical particles were nucleated every $5\,\mathrm{m}$ in an idealized atmosphere. Depending on the conditions at nucleation, the individual lifetime differs strongly (first plot). The lifetime is determined by the particle shape (third plot; $\Phi < 1$ plate-like, $\Phi > 1$ column-like) which strongly influences ice mass and sedimentation velocity (second and fourth plot).\\
 \\ \\
 Further extensions to the model are habit specific riming that allows the formation of graupel from columns, and plates, a habit-specific aggregation process, as well as secondary ice production mechanisms like rime splintering and freezing fragmentation.\\ Further extensions to the model are habit specific riming that allows the formation of graupel from columns, and plates, a habit-specific aggregation process, as well as secondary ice production mechanisms like rime splintering and freezing fragmentation.\\
-\\ + 
-{{  imprint_figur4.png?direct&550  }} +<met figure 
-\\ +    src="https://www2.meteo.uni-bonn.de/spp2115/lib/exe/fetch.php?media=projects:imprint_figur4.png" 
-<WRAP tablewidth 60% center>**Figure 4:** Temperature-dependent mass growth after 10 min of vapor deposition. The black line shows the results for a crystal that can grow asymmetrical, grey line for a spherical crystal. Blue open squares are measurements from Takahashi et al. (1991).</WRAP>\\ +    width="550" 
-\\ +    fit="responsive" 
-{{  imprint_figur5.png?direct&550  }} +    title="Figure 4" 
-\\ +    caption="Temperature-dependent mass growth after $10\,\mathrm{min}$ of vapor deposition. The black line shows the results for a crystal that can grow asymmetrical, grey line for a spherical crystal. Blue open squares are measurements from Takahashi et al. (1991)." 
-<WRAP tablewidth 60% center>**Figure 5:** Time series of height z, mass m, aspect ratio Φ, and terminal velocity vt for particles released every 5m between 3000m and 5000m altitude.</WRAP>\\+    caption-align="left" 
 +    load-animation="zoom-in" 
 +    background="white" 
 +    zoomable lightbox> 
 + 
 +<met figure 
 +    src="https://www2.meteo.uni-bonn.de/spp2115/lib/exe/fetch.php?media=projects:imprint_figur5.png" 
 +    width="550" 
 +    fit="responsive" 
 +    title="Figure 5" 
 +    caption="Time series of height $z$, mass $m$, aspect ratio $\Phi$, and terminal velocity $v_\mathrm{t}$ for particles released every $5\,\mathrm{m}$ between $3000\,\mathrm{m}$ and $5000\,\mathrm{m}$ altitude." 
 +    caption-align="left" 
 +    load-animation="zoom-in" 
 +    background="white" 
 +    zoomable lightbox>
 \\ \\
 \\ \\
  • projects/imprint.txt
  • Last modified: 2026/09/12 20:44
  • by ayush