Articles | Volume 14, issue 6
Atmos. Meas. Tech., 14, 4375–4402, 2021
https://doi.org/10.5194/amt-14-4375-2021

Special issue: Aeolus data and their application (AMT/ACP/WCD inter-journal...

Atmos. Meas. Tech., 14, 4375–4402, 2021
https://doi.org/10.5194/amt-14-4375-2021

Research article 14 Jun 2021

Research article | 14 Jun 2021

A new lidar design for operational atmospheric wind and cloud/aerosol survey from space

A new lidar design for operational atmospheric wind and cloud/aerosol survey from space
Didier Bruneau and Jacques Pelon Didier Bruneau and Jacques Pelon
  • LATMOS/IPSL, Sorbonne Université, UVSQ, CNRS, Paris, France

Correspondence: J. Pelon (jacques.pelon@latmos.ipsl.fr)

Abstract

Global wind profile measurement has, for a long time, been a first priority for numerical weather prediction. The demonstration, from ground-based observations, that a double-edge Fabry–Pérot interferometer could be efficiently used for deriving wind profiles from the molecular scattered signal in a very large atmospheric vertical domain has led to the choice of the direct detection technique in space and the selection of the Atmospheric Dynamics Mission (ADM)-Aeolus by the European Space Agency (ESA) in 1999. ADM-Aeolus was successfully launched in 2018, after the technical issues raised by the lidar development had been solved, providing the first global wind profiles from space in the whole troposphere. Simulated and real-time assimilation of the projected horizontal wind information was able to confirm the expected improvements in the forecast score, validating the concept of a wind profiler using a single line-of-sight lidar from space.

The question is raised here about consolidating the results gained from ADM-Aeolus mission with a potential operational follow-on instrument. Maintaining the configuration of the instrument as close as possible to the one achieved (UV emission lidar with a single line of sight), we revisit the concept of the receiver by replacing the arrangement of the Fizeau and Fabry–Pérot interferometers with a unique quadri-channel Mach–Zehnder (QMZ) interferometer, which relaxes the system's operational constraints and extends the observation capabilities to recover the radiative properties of clouds. This ability to profile wind and cloud/aerosol radiative properties enables the meeting of the two highest priorities of the meteorological forecasting community regarding atmospheric dynamics and radiation.

We discuss the optimization of the key parameters necessary in the selection of a high-performance system, as based on previous work and development of our airborne QMZ lidar. The selected optical path difference (3.2 cm) of the QMZ leads to a very compact design, allowing the realization of a high-quality interferometer and offering a large field angle acceptance. Performance simulation of horizontal wind speed measurements with different backscatter profiles shows results in agreement with the targeted ADM-Aeolus random errors, using an optimal 45 line-of-sight angle. The Doppler measurement is, in principle, unbiased by the atmospheric conditions (temperature, pressure, and particle scattering) and only weakly affected by the instrument calibration errors. The study of the errors arising from the uncertainties in the instrumental calibration and in the modeled atmospheric parameters used for the backscattered signal analysis shows a limited impact under realistic conditions. The particle backscatter coefficients can be retrieved with uncertainties better than a few percent when the scattering ratio exceeds 2, such as in the boundary layer and in semi-transparent clouds. Extinction coefficients can be derived accordingly. The chosen design further allows the addition of a dedicated channel for aerosol and cloud polarization analysis.

1 Introduction

Direct wind profiles in the meteorological atmosphere (0–25 km) are lacking over the oceans and in the tropics as indirect retrievals from temperature sounding are of no help in this region due to the lack of geostrophic equilibrium. The first priority in global atmospheric observations from space for weather forecasting was set on wind profiling to obtain better information on atmospheric circulation (Baker et al., 1995, 2014; WMO, 1996, 2012; Stoffelen et al., 2005, 2020).

Aerosols are good tracers of atmospheric dynamics as their reduced Brownian motion allows one to perform high-accuracy spectral measurements from the analysis of small Doppler shifts induced in lidar backscattered light. This is why the choice of heterodyne lidar was first targeted for space missions (LAWS, 1987; Baker et al., 1995). The feasibility of such heterodyne systems operating on particle scattering was discussed for a long time in the science community, but an important drawback was that the vertical profiling extent was limited by the very low value of the backscatter coefficient of the upper tropospheric particles in the infrared region. This leads to a very constraining lidar design in terms of the mass and power needs for such a space operating system. Such studies were continued to examine solutions and contributions of a space-based Doppler lidar possibly operating in direct detection (Baker et al., 2014).

Lidar backscattered signal from molecules, though much more spectrally broadened due to their high-speed thermal motion at molecular scale, was shown to be very effective for deriving upper tropospheric and stratospheric winds using direct detection. This was evidenced from pioneering work performed at Service d'Aéronomie, now called Laboratoire ATmosphères, Milieux et Observations Spatiales (LATMOS; Chanin et al., 1989; Garnier et al., 1992). Specific interferometric techniques involving multi-Fabry–Pérot in differential detection, also known as the double-edge technique, were implemented to analyze Doppler shift due to mean atmospheric motions. A few drawbacks are inherent to this approach, such as requiring a narrow field of view and a particulate scattering correction in the analysis to reduce biases (Garnier, 1990). For the first lidar space mission proposed to the European Space Agency (ESA), wavelength operation was selected in the ultraviolet (UV) region because of eye-safety issues and because it maximized molecular return. Though first observational tests in the UV region from space revealed their difficulty (McCormick et al., 1993), the candidate Atmospheric Dynamics Mission (ADM) was accepted as the first Earth Explorer mission by ESA in 1999. A technique combining two interferometers in cascade, with one matched to the narrow aerosol spectrum (Mie channel) and the other matched to the broad molecular spectrum (Rayleigh channel), was chosen to be implemented in the spaceborne Atmospheric LAser Doppler INstrument (ALADIN), providing a high signal-to-noise ratio over the whole atmosphere. An airborne demonstrator was developed and showed that the required performance could be achieved (Reitebuch et al., 2009; Lux et al., 2020). The satellite launch occurred in 2018, after a rather long delay induced by the large number of problems to be overcome. Though recent data analyses (Witschas et al., 2020; Martin et al., 2021) show that the horizontal line-of-sight (HLOS) wind measurements exhibit seasonal and orbital dependent biases slightly larger than the missions requirements, the measurements were confirmed to be highly beneficial and the European Centre for Medium-Range Weather Forecasts is now using them in their forecasts (Aeolus-ESA-Portal-forecast, 2020). The success of the Aeolus mission is then validating the concept of space-based wind measurements using high spectral Doppler analysis on backscattered molecular signals.

Other priorities in atmospheric observation from space have been identified on the retrieval of aerosol and cloud radiative parameters as well as precipitation, which are addressing meteorological and climate studies (Stephens et al., 2002, 2018; Illingworth et al., 2015; National Academies of Sciences, Engineering, and Medicine, 2018). This need has led to new observations from space, such as those proposed by the NASA-CNES (Centre national d'études spatiales) Cloud-Aerosol Lidar and Infrared Pathfinder Observations (CALIPSO) mission (Winker et al., 2010) launched in 2006 and still in operation for the survey of aerosol and cloud properties and their radiative impact. It had also stimulated the development of the high spectral resolution lidar (HSRL) technique for atmospheric studies from ground and from aircraft, as HSRL offers the capacity for retrieving the particle extinction and backscatter coefficients without using a priori assumptions. After the first pioneering developments using Fabry–Pérot interferometers (Shipley et al., 1983; Sroga et al., 1983), the first operational airborne HSRL systems were developed in the USA at the University of Wisconsin (Eloranta et al., 2008) and at NASA (Hair et al., 2008), as well as in Europe at the German Aerospace Center (DLR; Esselborn et al., 2008), with all of these systems being based on the iodine cell absorption technique. The new NASA Langley Research Center (LaRC) HSRL-2 system now also operates at 355 nm, using a Michelson interferometric technique that was used for multispectral aerosol characterization (Müller et al., 2014). Our first airborne backscatter lidar was developed in the 1990s in the frame of the French CNES-CNRS (National Center for Scientific Research) project LEANDRE (Lidar pour l'Etude des Aérosols des Nuages et Du RayonnEment) for atmospheric studies. Since it was operating at similar wavelengths, it was involved in the validation of the Cloud-Aerosol Lidar with Orthogonal Polarization (CALIOP)-CALIPSO observations of cirrus clouds (Mioche et al., 2010). It was then upgraded to add a high spectral resolution (HSR) channel and renamed as LEANDRE-New Generation (LNG). In contrast to the DLR and NASA systems, the French multi-wavelength system LNG was designed to operate as a HSRL at 355 nm for aerosol/cloud profiling, with an added Doppler capacity for wind measurements. The HSR Doppler (HSRD) lidar design is based on the use of a single Mach–Zehnder interferometer (MZI) with four detection channels in phase quadrature (Bruneau and Pelon, 2003; hereafter BP03). It was chosen to better meet the objectives of combined radar–lidar atmospheric observations (Delanoë et al., 2012). HSRD-LNG observations have been successfully validated and involved in several field experiments, including the Aeolus Cal/Val and the Earth Cloud, Aerosol and Radiation Explorer (EarthCARE) preparation (Bruneau et al., 2015; Schäfler et al., 2018; Cazenave et al., 2019). In the United States, Ball Aerospace developed a Doppler wind lidar including a spectral discriminator based on the same principle of the quad-channel MZI (Grund et al., 2009), which was successfully operated on board the NASA WB57 aircraft (Tucker et al., 2018) and further involved in the Aeolus Cal/Val (Tucker et al., 2019, 2020).

The successes of the Aeolus and of the CALIPSO missions have proved the potential of lidar sounding from space and its importance for meteorological and climatological applications. Many technical challenges for UV operation within Aeolus have now been overcome by Airbus Defense and Space and ESA that paved the way for the EarthCARE mission focused on clouds and aerosols. This mission, developed in collaboration with the Japanese Space Agency, is to be launched by the ESA in 2022. The EarthCARE payload, embarking on a UV HSRL ATmospheric LIDar (ATLID) and a new cloud radar, should extend and improve upon CALIPSO backscatter lidar and CloudSat radar instruments. These missions are designed for radiation budget analysis through the retrieval of cloud and aerosol properties (Illingworth et al., 2015; Stephens et al., 2018).

Taking advantage of observed performance and measurement capabilities from airborne measurements based on the HSRD-LNG system, we study in this paper a MZI-based system for a future operational space mission. The proposed design is aimed at a performance-improved operation of a UV spaceborne lidar addressing atmospheric dynamics as a first goal. The selected MZI design may also contribute to a continued radiation budget analysis after the CALIPSO-CloudSat and EarthCARE missions. The paper is organized as follows: in Sect. 2, we recall the choices that are to be made to meet wind profiling objectives, and in the following section, we develop the lidar design and present its main characteristics, discussing its advantages. The performance assessment of the MZI-based system is then presented and discussed in a comparative way in Sect. 4, whereas Sect. 5 presents the final considerations in a short discussion.

2 Preliminary choices

As previously introduced, the requirement of acquiring high-accuracy wind profiling over a broad vertical atmospheric domain is ruled by the selection of efficient Doppler analysis on the molecular backscattered signal. Only molecular scattering can provide a high signal-to-noise ratio (SNR) in lidar detection in the upper troposphere and stratosphere at the global scale. Such a capacity has proven to be of high importance to Numerical Weather Prediction (Baker et al., 2014; Le Pichon et al., 2015; Rennie and Isaksen, 2020). As the intensity of the Rayleigh scattering cross section is inversely proportional to the fourth power of the emission wavelength, the use of a UV system is preferred to optimize lidar profiling.

The ADM-Aeolus main requirements are based on this approach of performing accurate wind measurements in clear air over the whole troposphere (ESA, 1999). The Aeolus instrument is based on newly developed narrow line UV solid state laser source, and takes advantage of the direct detection of high molecular scattering signals at 355 nm through a large diameter telescope and a cascade spectral interferometric discriminator complemented by high efficiency detectors (Aeolus-ESA-Portal-mission, 2002; ESA, 2008). The use of high-performance Accumulation Charge Coupled Devices (A-CCDs) in ALADIN offers a very high efficiency (above 75 %) and a low read noise, which allow near-quantum noise limited detection in the UV. The ALADIN design is, thus, meeting most of the needs for wind measurement, but operation has revealed performance constraints set by the interferometer choice.

The first wind measurements by lidar on molecular scattering have been performed at the Observatoire de Haute Provence (OHP) in the upper atmosphere with a double-edge (DE) technique using a Fabry–Pérot interferometer (FPI; Chanin et al., 1989; Garnier et al., 1992). This photometric differential technique uses two spectral channels precisely positioned on each side of the molecular spectrum. Temperature and pressure are significantly varying on the vertical in the atmosphere, and the dependence of the molecular spectral broadening with temperature and pressure needs to be accounted for in the analysis process (Dabas et al., 2008; Zhai et al., 2020). Particulate backscattering can, furthermore, contribute to within a few percent and even more in the troposphere. This has been shown to be a constraint for DE-FP techniques, requiring independent backscatter ratio measurements for bias correction (Souprayen et al., 1999a, b; Witschas et al., 2020). In addition to the DE-FP of the Rayleigh channel dedicated to the analysis of the molecular return, ALADIN uses a Fizeau interferometer for the Mie channel dedicated to the analysis of particulate backscattering. An important question in the optical design of the interferometers is to match the aperture of the telescope without degrading the overall performance in case of misalignment. Both DE-FP and Fizeau interferometers have a small angular acceptance. The optical adaptation of the interferometers to the large telescope aperture results in a very small field of view and imposes a high-accuracy requirement on the transmitter–receiver co-alignment. The solution used in ALADIN is to take advantage of the large telescope magnification for both the emission and the reception to reduce alignment sensitivity. The emission beam is sent through the telescope using a polarization bypass to separate emission and reception paths (Aeolus-ESA-Portal-mission, 2002). A drawback of this optical design is that only the backscattered light co-polarized with the emission can be detected. This leads to significant losses in the detection of particulate backscattered signal in the case of dust and ice crystals that are inducing large depolarization. It also introduces an important limitation in the retrieval of the aerosol and cloud parameters using the analysis of the Fizeau interferometer A-CCD channels (Flamant et al., 2008).

The two-wave interferometers such as Michelson (MI) or Mach–Zehnder (MZ) interferometers are a second group of techniques that can be used in Doppler lidar measurements. MI and MZ interferometers in photometric or fringe imaging modes have already been proposed in HSRL systems for wind measurements or scattering analysis (Bruneau, 2001; BP03; Cézard et al., 2009; Liu et al., 2012; Bruneau et al., 2015; Cheng et al., 2015; Herbst and Vrancken, 2016; Tucker et al., 2018). These interferometers can include a field compensation design (Bouchareine and Connes, 1963), which allows a large incident field angle and facilitates their accommodation with a large-beam étendue system (i.e., a large-sized telescope and a relatively wide field angle; see Appendix B for further discussion). MI and MZ interferometers can be designed to operate with two or four detection channels (Bruneau, 2001). Dual channel techniques are very similar to the DE-FP and present the same limitations due to their sensitivity to temperature, pressure, and aerosol scattering. The quadri-channel detection technique (BP03), which provides four signals in phase quadrature, allows independent determinations of interference modulation and phase, with the wind measurements being derived from the interference phase. Both particulate and molecular returns produce the same interference phase and, therefore, the same wind measurement. Particulate backscattering thus improves the SNR and the wind speed accuracy without introducing bias. It can also appear convenient to use the linear fringe's interferometric pattern imaged on a CCD array, as its position depends linearly on the Doppler shift (Herbst and Vrancken, 2016). It has been shown that fringe imaging and quadri-channel techniques provide the same theoretical measurement precision (Bruneau, 2002; BP03). It must be also considered that the accommodation of linear fringes on a square image zone with a circular aperture receiver necessitates a truncation of the aperture that would decrease the signal and, hence, the measurement precision. We, therefore, rule out the fringe imaging technique from our choices.

In addition, the quadri-channel techniques offer another advantage as they do not require any specific spectral positioning of the laser emission relative to the interferometer, provided that a reference signal characterizing the frequency at the emission is acquired. Appropriate frequency stability is just required during the signal accumulation needed for a single measurement. A large spectral drift of the laser source and the interferometer is tolerated over a longer timescale. Off-axis MI interferometer (Liu et al., 2012) operation associated with quadri-channel detection presents the same advantages in terms of measurement robustness, i.e., insensitivity on molecular spectral shape and particulate backscattering and tolerance with regard to spectral drifts and misalignments (thanks to a field-compensated design). Although the MZ optical arrangement is slightly less simple than the off-axis MI's, the latter brings the difficulty that one output port is necessarily very close to the input one and would hamper the positioning of the detectors. The QMZ technique, thus, appears as a near-optimal choice in this group, and we made this choice to optimize the new receiver design.

An experimental comparison has been performed between the dual-channel MZ (DMZ) and the DE-FP techniques at the OHP (Bruneau et al., 2004). It was shown that, under the same conditions of measurement, the DMZ statistical error is lower than that of the DE-FP by a factor of 1.4 thanks to a higher optical efficiency (factor of 2). As the quadri-detection MZ (QMZ) produces a statistical error larger than that of the DMZ by the same factor (Bruneau, 2001), the QMZ and the DE-FP are equivalent in terms of statistical error. It is to be further noted that an optimized and original optical design is used in ALADIN; the reflected signal from one edge of the DE-FP interferometer is reinjected into the other edge. This scheme improves the DE-FP optical efficiency as compared to the common method that splits the incident signal onto the two halves of the FP aperture, as done in the OHP setting. It leads to a theoretical advantage for the ALADIN concept in terms of measurement precision, as compared to the OHP DE-FP (and, consequently, to the quadri-detection technique) by a factor that depends on the efficiency of the double-pass optical setting but cannot be larger than 1.4 (limited case of a factor 2 gain in the transmitted energy).

A comparison of the advantages and disadvantages guiding the choice of interferometric design for wind measurement on the molecular scattering is summarized in Table 1. In contrast with ALADIN, which utilizes a second interferometer (Mie channel) for regions of the atmosphere where the aerosol load is significant, and taking advantage of the QMZ insensitivity to particulate backscattering (in terms of bias), we chose to use a unique interferometer to probe all the layers of the atmosphere. This choice allows a simplified receiver design considered to ensure good robustness and reliability. In the conducted analysis, we will rely on numerical simulations and on the results obtained from the QMZ operation with the airborne HSR-LNG to define realistic parameters for the interferometer and derive the performance assessment.

Table 1Summary of advantages (+) and disadvantages () of measurement techniques for direct detection wind profiling on molecular return.

Download Print Version | Download XLSX

An additional advantage of the QMZ technique is that it also allows measurements of the scattering ratio (ratio of the total to molecular backscatter coefficients derived from the contrast of the interference). Provided the emission linewidth is sufficiently narrow, the particulate signal produces an interference contrast near unity, which is significantly higher than that produced by the molecular signal (see Appendix A; Eq. A14). The measurement of the interference contrast given by the total atmospheric signal then leads directly to the scattering ratio and, from there, to a precise quantification of the aerosol backscatter coefficient. We will come back to this advantage for the analysis of aerosol and cloud properties.

3 Lidar design

3.1 General architecture and characteristics

As mentioned earlier, the goal for the new design is to simplify and ruggedize the existing one as much as possible, keeping as many solutions based on Aeolus and ATLID designs as needed and accounting for recommendations made by the Aeolus Science Advisory Group (ASAG, 2020). The transmitter is, thus, based on the nominal Nd:YAG laser in a redundant design, with frequency converters to 355 nm, as developed for Aeolus. As the field-compensated MZI acceptance angle is much wider than that of the DE-FP, a very small emission divergence and a monostatic transmitter–receiver is no longer required. So, in contrast to ALADIN, but similar to the ATLID lidar for EarthCARE (Hélière et al., 2012), a bistatic design is chosen. The schematic of the lidar optical design is presented in Fig. 1. The lasers can be coupled to a small telescope (typically about 15 cm in aperture) that assures an emitted beam divergence of 50 µrd for a 99 % relative encircled energy. The lasers and the expanders can be mounted on the same plate, as was done on CALIPSO, and boresight mirrors can be tilted to maintain alignment with the receiving optics. The emitted energy will conservatively be kept similar to the actual ALADIN laser source (e.g., 65 mJ at 355 nm). We, however, will extrapolate, with little risk, the possibility of extending the laser repetition rate to 100 Hz. A short laser pulse duration of 5–7 ns (corresponding to a high-energy extraction from a Q-switched oscillator and leading to a high-frequency conversion efficiency) is allowed to keep an appropriate spectral linewidth (less than 150 MHz). We will also assume that the pulse linewidth and the spectral jitter or drift allows the maintenance of the average spectral width to be within 200 MHz during an accumulation of 50 shots, as observed in spaceborne Aeolus observations (Reitebuch et al., 2020).

The receiver telescope, with a 1.5 m aperture, is coupled to a silica–silica optical fiber through an assembly of front optics, which includes a 0.1 nm bandwidth background filter. The signal fiber, with a core diameter of 340 µm (and a numerical aperture of 0.22) is used as the field stop and defines a reception field angle of 100 µrd, which allows a good margin for the lidar emission–reception alignment. Note also that the receiver is not sensitive to the polarization state of the collected light and, hence, to the depolarization by particles scattering. As discussed in the literature, it could be useful to measure the particulate depolarization to better identify cloud and aerosol types as emphasized by the Aeolus Science and data quality Advisory Group (Aeolus SAG​; ASAG, 2020; see also, for example, Burton et al., 2012). This can be handled by inserting a polarization splitter between the telescope and the interferometer in the front optics system (see Fig. 1). The interferometric analysis is done, in this case, on the parallel polarized signal, and the perpendicularly polarized signal is measured in an additional channel, as done in the DHRS-LNG instrument (Bruneau et al., 2015). However, we will not discuss a polarization channel addition in the basic lidar design but rather keep it as an option. One could refer to Bruneau et al. (2015) for further information on this implementation.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f01

Figure 1Diagram of the lidar system. L1 and L2 – lasers (nominal and redundant); ET – emission telescope; BM – boresight mirror; RT – receiver telescope; FO – front optic (including background filter); SF – signal fiber; RF – reference fiber; FC – fiber coupler and mode scrambler; IO – input optic; MZI – Mach–Zehnder interferometer; OS – output separation optic; D1 and D2 – A-CCD detectors.

Download

An optical mode scrambler is inserted on the fiber path in order to obtain a uniform illumination distribution at the interferometer input independent of the illumination distribution in the telescope focal plane (field stop). The mode scrambler consists of two lenses; the first lens images the output of the first fiber on the second lens, while the second lens images the first lens aperture on the second fiber. In this way, the near and far fields at the output of the second fiber are uniform and fill the whole fiber beam étendue. This arrangement ensures that the interferometer response is not biased by transmitter/receiver misalignment. A small plate and a symmetrical lens arrangement inserted in the mode scrambler allows the injection of a small amount of the emitted pulse used as the reference signal and transported by a second optical fiber. The fiber and the scrambler ensure the complete depolarization of the signal before it arrives on the MZI (even when including a polarization splitter in the front optics). This was implemented and successfully tested on the airborne LNG system. The overall efficiency of the fibers and mode scrambler on the atmospheric signal path is around 80 %. The output of the fiber is then collimated by a 15 mm focal length lens at the MZI input port.

The main characteristics of the proposed lidar design are reported in Table 2 and compared to the nominal (Paffrath, 2006; Aeolus-ESA-Portal-mission, 2002) and actual (Reitebuch et al., 2020) ALADIN parameters (see also ASAG, 2020). This table also includes parameters discussed in the next subsections.

Table 2Main characteristics of the lidar design used for the analysis of performance. Parameters for the proposed system, compared to those from the on-orbit Aeolus, as reported by Reitebuch et al. (2020). Note: PBL is planetary boundary layer.

Download Print Version | Download XLSX

3.2 QMZ Design

The field-compensated QMZ design has been detailed in several papers (Bruneau, 2001; BP03; Smith and Chu, 2016; Tucker et al., 2018). Making the choice of a unique interferometer, the optical path difference (OPD) Δ between the two arms of the interferometer is the key parameter for optimizing the wind speed retrieval over the whole troposphere using both the molecular and the particulate backscattering. In contrast with BP03, who focused mainly on the HSR separation of molecular and particulate backscattering, here we give priority to the optimization with regard to wind measurement and consider the particulate backscatter coefficient as a by-product (though of great interest). We will then consider the performance obtained on the analysis of aerosol and cloud properties for this wind-performance-driven design.

The principles of the lidar interferometric system are presented in Fig. 2a. The optical signal incident on the interferometer is previously depolarized by passing it through a multimode optical fiber. A quarter-wave plate is inserted into one arm of the interferometer, and polarizers at its output separate the signal in four interference components in phase quadrature.

The interferometer is built in the same way as for the HSR-LNG (Bruneau et al., 2015), with an assembly of fused silica prisms and plates (Fig. 2b). For the selected MZ optical path difference (see the next section), the total prism assembly stands within a volume of approximately 1.5 cm ×2 cm ×4 cm. The different elements can be optically contacted resulting in a single block interferometer. The interferometer adjustment is obtained by construction and is unalterable.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f02

Figure 2(a) QMZ schematics. BS – beam splitter; M – mirror; CP – field compensation plate; QWP – quarter-wave plate; WP – Wollaston polarizer; D1 and D2 – A-CCD detectors. (b) MZ actual prism arrangement (QWP, WP, and detectors are not shown here).

Download

An alternative design of a field-compensated MZI is given by the cat eye arrangement (Tucker et al., 2018). This fully reflective design eliminates the light path through the glass, which can cause a wavefront distortion but leads to a bulkier arrangement which requires high mechanical stability. On the opposite side, the all-prism MZI design is insensitive to vibrations but is sensitive to temperature gradients. Nevertheless, as discussed in Sect. 3.4, for a small OPD, the all-prism design can achieve high quality, and the thermally induced wavefront distortion can be easily controlled. As mentioned above, the MZI can be replaced by an off-axis Michelson interferometer but still in quadri-channel detection. In this case, the quarter-wave plate should be replaced by a eighth-wave plate used in double path. A difficulty of this design is the accommodation of one detector close to the input port of the interferometer (the off-axis angle must be small in order to achieve a field compensation without residual wavefront distortion). An additional fiber between the interferometer and the detector could be a solution. The alternative choice of a quadri-channel, off-axis Michelson interferometer would lead to the same equations and results. In this paper, we, however, keep considering the QMZ as being the nominal design, as we refer to proven optical solutions from our airborne system.

The beam issued from each of the two MZI output ports is focused on an A-CCD detector by means of a 6.5 mm focal length lens. A quartz Wollaston polarizer, positioned just ahead of the focusing lens, separates the two polarizations issued from one MZI output port, with an angular separation angle of 25 mrd. In this way, the fiber output is imaged on the detector as two spots of 150 µm in diameter separated by 160 µm. Thanks to the mode scrambler, these images are well-defined disks of homogeneous illuminations. Each spot fills an 8 by 8 pixel area in the A-CCD image zone in the same way that the Rayleigh channel of ALADIN does. The two A-CCD image zones provide the four channel signals (Eq. 1) of the QMZ technique.

The average signal delivered by each channel of the A-CCD outputs, for i=1 to 4, can be written as follows:

(1) S i = S tot 4 a i 1 + M i M atm sin φ + i - 1 π 2 + S b i ,

with Stot as the total signal and ai, Mi as the relative photometric sensitivity and instrumental interference modulation of channel i, respectively. Matm is the interference modulation given by the atmospheric backscattered signal, and φ is the interference phase. Sbi is the background signal due to solar-detected light and A-CCD intrinsic noise.

The interference phase, from which the wind speed is derived, and the interference modulation, which leads to the scattering ratio, can be determined independently from these four signals. Actually, the line-of-sight (LOS) wind speed is calculated from the phase difference between the atmospheric signal and a reference signal obtained on a highly attenuated pick up of the emission.

The equations which give the wind and backscatter products, and the respective random errors, are detailed in Appendix A. These equations are the basis of numerical simulations that have been performed to analyze the measurement performance of the selected design. The statistical error on wind depends on the OPD and interference modulation (see Appendix A). We will first examine the optimal determination of these two parameters more directly linked to the interferometer design and then discuss (in Sect. 4) the measured SNR, depending on the lidar system and mission parameters, as derived from the numerical simulations performed.

3.3 QMZ optical path difference

As seen from Eq. (A16) in Appendix A, the statistical error on wind measurement for a given SNR is inversely proportional to the OPD and to the interference modulation Matm. The interference modulation Matm is, in counterpart, a fast-decreasing function of the OPD for a given signal spectral width. A compromise is thus to be achieved between the frequency discrimination (large OPD) and the interference modulation (small OPD). It has been shown (Bruneau, 2001) that, for measurements in a purely molecular atmosphere at λ=355 nm, the optimum OPD is 3.2 cm. As we want to optimize measurement in conditions of clean air (scattering ratio smaller than 1.01), the OPD should be close to this value. The optimal OPD is thus quite a lot smaller than the one proposed in BP03 (10 cm) that aimed to compromise between wind and scattering ratio measurements. A complete parametric study is presented in Sect. 4. Such a small OPD MZI can be easily integrated as a solid-state device derived from the design used for the airborne system (Bruneau et al., 2015), as reported in Fig. 2b.

For a 3.2 cm OPD, the modulation produced by the molecular return Mmol is dominated by the Doppler spectral width of the thermal motion of molecules and varies from 0.49 to 0.59, depending on the atmospheric temperature, with an average value of 0.56. Note that, at high atmospheric pressure near the surface, Brillouin molecular scattering causes a relative broadening of this spectrum by approximately 1.7 %. This effect itself causes a small decrease in the molecular modulation Mmol from 0.49 to 0.48. As the spectral broadening caused by the particle Brownian motion is small compared to the emitted linewidth, the modulation produced by the particle return Mpar is very close to that given by the emitted linewidth. For an emission linewidth of 200 MHz, including the broadening by frequency shift or jitter during the measurement integration duration, and a 3.2 cm OPD, Mpar is still as high as 0.95, according to the equations given in BP03.

Note again that, as the QMZ technique allows the determination of wind speed (through the interference phase) and the scattering ratio (though the interference modulation) independently, the superposition of a narrow particle spectrum to the wide molecular spectrum does not bring any measurement bias. The increase in interference modulation caused by an additional particle scattering will indeed improve the wind measurement accuracy.

3.4 QMZ optical quality

The interferometer optical quality is obviously an important aspect of the design as it determines the intrinsic modulation factors Mi (Eq. 1). These modulation factors can be slightly different from one channel to the other, but for clarity, we consider here that they are all equal to M0. The equations of Appendix A show that the random errors (both in wind speed and scattering ratio) are, at first order, inversely proportional to this intrinsic modulation factor M0.

We can also consider that M0 is the product of two factors, i.e., MW is the modulation degradation caused by imperfections of optical surfacing and non-homogeneities of the optical index resulting in a global wave front error (WFE), and MR is the modulation degradation caused by the imbalance of the reflection–transmission factors of the beam splitters.

It has been shown that the modulation degradation of a Michelson interferometer is a function of the root mean square (RMS) value of the WFE (σWFE), which is almost independent of the shape of this distortion (Liu et al., 2012). This result is obviously also valid for a MZI. Assuming a Gaussian distribution of the WFE, we obtain the modulation factor MW as follows:

(2) M W = 1 σ WFE 2 π exp - δ 2 2 σ WFE 2 cos 2 π δ λ d δ .

We can also admit that σWFE is proportional to the area of the useful interferometer aperture. It is, therefore, essential to evaluate the useful aperture of the MZI, which can withstand the large beam étendue of the system. The calculation, detailed in Appendix B, leads to the chosen lidar parameters to a useful aperture DMZI=6.2 mm.

Using Eq. (2), we calculate MW as a function of the MZI aperture for different values of the σWFE per square centimeter and an operation wavelength of 355 nm (Fig. 3a). For comparison, the intrinsic instrumental contrast of the HSRD-LNG interferometer is 0.65 for a useful aperture of 20 mm (and a 20 cm OPD) that corresponds to a σWFE less than 20 nm cm−2. For the same optical quality σWFE=20 nm cm−2 (which can be nonetheless improved), a modulation factor MW>0.99 is achievable for the proposed MZI, with a useful aperture of 6.2 mm (see Fig. 3a).

In the case of a non-homogeneous temperature distribution in the optical elements, and more particularly a transverse temperature gradient in the compensation plate, leading to an angular tilt of one wavefront plane, we computed that the impact is an additional degradation of about 0.5 % in MW for a thermal gradient of 0.1 K cm−1. This shows a relative acceptance of temperature changes, which do not require a high standard in the temperature control of the interferometer.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f03

Figure 3(a) Instrumental modulation factor MW as a function of MZI useful aperture for different RMS WFE. The dots represent the MZI of the present study and the actual MZI of HSRD-LNG. (b) Instrumental modulation factor MR as a function of the beam splitter RT difference.

Download

Note also that, for our on-axis, field-compensated design, the variation in OPD is only dependent on the fourth power of the source angle (the second power dependence is canceled, and the third order dependence is null due to all on-axis optical elements). With the system parameters presented above, the source full angle brings a negligible contribution of less than 0.1 nm to the RMS WFE (see Appendix B).

The second intrinsic modulation factor MR stems from the fact that it is not possible for a pure (non-absorbing) dielectric coating to ensure a perfect balance between the reflectivity R and the transmission T for both polarizations at an incidence angle of several tens of degrees. The consequent imbalance of the beam splitter reflectivity causes a modulation factor MRmin=2RTR2+T2 on two of the four channels of the QMZ, with the other two channels being unaffected. The average reflectivity modulation factor is then MR=12R2+T2. Figure 3b presents the decrease in instrument intrinsic modulation MR as a function of the reflectivity transmission difference RT. For comparison, in the HSRD-LNG interferometer, the incidence angle on the beam splitters is 40 and a reflection transmission imbalance of 0.1 has been achieved, leading to MR=0.99.

We can then conclude that an intrinsic instrument modulation M0=0.98 is achievable for a MZI of a small OPD (3.2 cm) associated to a spaceborne lidar with a receiver aperture and field angle product as large as 0.15 m mrd−1.

Note also that the optical quality requirements on the MZI are less stringent than for a FPI, which necessitates a larger aperture, because of the low field angle acceptance and a high surfacing quality to avoid losses in transmission and finesse.

3.5 QMZ calibration

Prior to processing the actual atmospheric signals, it is necessary to perform a calibration of the MZI to determine the transmission and modulation factors ai and Mi of the MZI defined in Eq. (1). The sensitivity parameters ai can be determined by recording the four QMZ signals in the absence of interference, either by sequentially masking one arm of the interferometer and then the other and adding the signals of the two sequences or by using the laser in multimode operation (without injection seeding) to obtain a flat interferometric response. The calibration of the instrumental modulations Mi is then obtained by recording a long sequence of reference signals with a slowly varying OPD phase (with temperature, for instance) or by tuning the laser seeder frequency. The recorded signals are fitted by a least square method on the four modeled signals (Eq. A2) by adjusting the Mi parameters.

An error in the determination of the instrumental sensitivities ai and instrumental contrasts Mi propagates to the calculation of the complex signal Q (Eq. A4) and then to the LOS velocity and scattering ratio measurements. These calibration errors apply equally on the reference complex signal Qr but with a slightly different impact due to a different modulation factor and to the Doppler phase shift. The consecutive measurement errors are interference-phase dependent, with a negligible averaged value, but with a perceptible amplitude.

We will discuss the calibration obtained from the results from the airborne HSRD-LNG observations during previous field experiments in Sect. 4.3. The impact of calibration errors on the simulation of new spaceborne measurements is further discussed in Sect. 4.6.

4 Performance assessment

4.1 Model description

Performance modeling starts by computing the total signal Stot (Eq. 1) expressed in number of photo-electrons (p-e) for a single shot and is based on the following canonical lidar equation:

(3) S tot ( R ) = η E A T inst h ν r = R - δ R / 2 r = R + δ R / 2 T atm 2 ( r ) β ( r ) r 2 d r ,

where R (meters) is the range from the instrument, δR (meters) is the range gate, η is the detector quantum efficiency, E (joules) is the emitted energy, A (square meters) is the receiver aperture area, Tinst is the total optical efficiency product of transmitter and receiver efficiencies, hν is the emitted photon energy, Tatm is the atmospheric transmission from instrument to range r for a line-of-sight (LOS) nadir angle θ, and β (inverse meters per steradians) is the total (molecular and particulate) backscatter coefficient.

The atmospheric backscattering and transmission are computed from the ESA reference model of atmosphere (RMA), including a measurement statistic of aerosol backscatter coefficients (Vaughan et al., 1998). A cirrus cloud between 9.5 and 10.5 km altitude, with an optical thickness of 0.1 (backscatter coefficient equal to 4×10-6 m−1 sr−1), can also be introduced. The RMA comprises data of different aerosol and cloud backscatter coefficients and extinction, background radiance, and ground albedo. Extinction and backscatter coefficients corresponding to the lower quartile (LQ), median (MD), higher quartile (HQ) and median profiles with an additional cirrus cloud (MD+CIR) are given in Fig. 4 for the 355 nm operation wavelength.

A background signal Sbs caused by the Sun's illumination and the intrinsic read noise Sbd due to the A-CCD detector are added on all the range gates so that the total background noise is written as follows:

(4) S b = S bs + S bd = η A Ω T rec I s ( λ ) δ λ cos ( θ s ) alb π T atm ( θ s , z s ) T atm θ , z s 2 δ R c + S bd ,

where Ω (sr) is the receiver field solid angle, Trec is the receiver efficiency, Is (W m−2) is the Sun irradiance at top of the atmosphere at wavelength λ, δλ is the bandwidth of the blocking filter, θs is the Sun elevation angle, alb is the albedo (surface or cloud), and zs is the altitude of the scattering layer. For these computations, we take alb=0.3 for land surface and add alb=0.015 for thin cirrus. Assuming a dawn–dusk Sun-synchronous polar orbit similar to Aeolus, we take θs=80. The blocking filter has a bandwidth δλ=0.1 nm. An important advantage of the A-CCD detectors is their high quantum efficiency (η=0.85) combined with a low read noise. The signal is pre-accumulated on 50 shots on the A-CCD (e.g., 0.5 s corresponding to an along-track horizontal sampling resolution of 3.6 km; similar to Aeolus) before being read by the analog-to-digital converter that adds a noise equivalent to a background signal Sbd of 6 p-e per detector pixel (Paffrath, 2006).

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f04

Figure 4Backscatter and extinction coefficients vertical profiles at 355 nm used in the performance model. (a) RMA lower quartile, (b) RMA median, (c) higher quartile, and (d) median plus cirrus.

Download

The signals are first accumulated on the A-CCD over 50 shots, forming an elementary sample. Then, 14 elementary samples are reference adjusted and accumulated, corresponding to a total of Ns=700 shots for an observation horizontal resolution of 50 km, and the resulting total SNR is as follows:

(5) SNR = S tot N s S tot + S b .

The recorded total signals and SNR (i.e., calculated on the sum of the four detection channels) vertical profiles used in the performance model are presented in Fig. 5 for the median (MD) RMA backscatter profile with the cirrus cloud and a 45 LOS angle. Except for a large increase in the cirrus cloud and at ground level, the SNR is slowly varying over the whole troposphere.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f05

Figure 5(a) Number of accumulated photo-electrons per range gate. (b) SNR for RMA MD backscatter profile plus cirrus at 45 LOS angle.

Download

The standard deviation on the projected horizontal line-of-sight (HLOS) wind speed is calculated from Eq. (A17) as follows:

(6) σ V HLOS = σ V LOS sin ( θ ) R E + z R E + z sat = c λ 4 π Δ sin ( θ ) 2 SNR 1 M 0 M atm R E + z R E + z sat 1 - M 0 2 M atm 2 4 ,

where RE is the Earth radius, and zsat is the satellite altitude.

The MZI intrinsic modulation is calculated assuming a σWFE of 20 nm cm−2, a RT imbalance of 10 %, and an emitted spectral width and jitter of 200 MHz RMS. The modulation on the molecular return Mmol is computed with the standard model of temperature at midlatitudes.

The background and the reference signals are assumed to be recorded with a SNR much higher than that of the atmospheric signal, so that they add a negligible variance to the measurements when subtracted from the total signal. This can be done on each acquisition sequence to avoid possible bias due to hot pixels, as observed and corrected with A-CCDs in space (Weiler et al., 2019).

The speckle noise is not an issue for the measurement accuracy, as the design is based on a large aperture and wide field of view. The receiver number of spatial speckles Ms, defined as the ratio of the solid angle of the transmitted beam to the diffraction solid angle of the telescope, is 2.75×104. The number of temporal speckles Mt is around 500, due to the extended range gates. The total number of speckles Mspec=Ms. Mt is then approximately 1.4×107. As the number N of collected photo-electrons per shot and range gate is on the order of 103, the speckle noise (given by the ratio N/Mspec) is much smaller than 1, so that the noise variance is not modified.

Note also that the fiber beam étendue is necessarily larger than the telescope beam étendue in order to accept the received beam with a substantial alignment margin. The maximum amount of spatial speckle of the fiber (9×104) is then larger than Ms and does not limit the total amount of speckle of the signal.

Appendix C shows measurements performed with HSRD-LNG, where the error calculated with equations similar to those used in the performance model is compared to the experimental error. Figure C1 shows that the calculated and experimental errors are in good agreement. A comparison between lidar wind measurements, including calculated error, and collocated radiosonde profiling is also presented in Appendix C (Fig. C2 and Table C1). A similar comparison of measured and calculated errors on the backscatter coefficient also shows a good agreement (Fig. C3). We can, therefore, consider that these results validate the equations used in the performance model.

4.2 OPD and LOS angle optimizations

We first come back to the OPD optimization to detail results previously given as averages. The standard deviation of the statistical error on the retrieved horizontal wind speed VHLOS, as given by Eq. (6), is presented in Fig. 6 for the median, higher quartile, and lower quartile of the aerosol backscatter coefficient distributions and for OPDs from 2.2 to 4.2 cm. The LOS angle is set to 45 in these computations. Figure 6d thus shows that the optimum OPD of 3.2 cm is effective for all atmospheric models corresponding to scattering ratios smaller than 2, as it is the case outside the boundary layer. We now look at the pointing angle. The standard deviation of the statistical error on horizontal wind speed is presented in Fig. 7 for the median, higher quartile, and lower quartile of the aerosol backscatter distributions and for LOS angle varied from 35 to 55. Results are analyzed (as for OPD) by looking at HLOS wind error averaged between 0.5 and 15 km and vertical profiles. The MZI OPD is set to 3.2 cm for these computations.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f06

Figure 6(a, b, c) Horizontal wind speed (HLOS) statistical error as a function of altitude for OPD for lower quartile, median, and higher quartile RMA aerosols distribution, respectively. (d) Wind speed error averaged between 0.5 and 15 km in altitude as a function of OPD.

Download

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f07

Figure 7(a, b, c) HLOS wind speed statistical error as a function of altitude for LOS angles between 35 and 55, for lower quartile, median, and higher quartile RMA aerosols distribution, respectively. (d) HLOS wind speed error averaged between 0.5 and 15 km in altitude as a function of LOS angle.

Download

As can be seen from Fig. 7d, the optimal 3.2 cm OPD and 40–47 LOS angles are well matched to aerosol distributions from lower to higher quartiles of RMA aerosol distribution. The errors are noticeably degraded in the troposphere below 10 km in altitude for angles smaller than 40 or larger than 50. For all the aerosol distributions, a LOS angle close to 45 appears to give better results. We, thus, chose 45 as the optimal value for conducting final analysis performance on HLOS wind retrievals. The standard deviation of the horizontal wind speed statistical error, averaged between 0.5 and 15 km in altitude, is slightly less than 2 m s−1 in the troposphere for the three distributions.

4.3 Comparison with Aeolus requirements

Figure 7a shows the HLOS wind speed error profiles for the selected parameters and the aerosols distributions LQ, MD, HQ, and MD plus cirrus for the parameters listed in Table 2, corresponding to the previously discussed choices and optimization. Figure 8b shows the same results but for a variable vertical resolution according to Aeolus requirements. The modeled statistical errors for the RMA MD aerosol distribution presented in the previous section are summarized in Table 4 in comparison with Aeolus requirements. It can be seen that, in the free troposphere, the Aeolus requirements are fulfilled with a good safety margin. For a constant vertical resolution of 500 m, results obtained in the atmospheric boundary layer are better than in the clean atmosphere, due to a larger scattering ratio which compensates for the decrease in transmission till the aerosol attenuation becomes too high. The errors are, nevertheless, slightly higher than the requirement (1 m s−1) in the planetary boundary layer (PBL), with values around 1.5 m s−1 on average.

In presence of a cirrus cloud, the wind speed accuracy is improved to a fraction of meters per second, due to the increased signal return and interference modulation Matm (Eqs. A3 and A12), but is degraded in clear air below the cloud layer by 0.5 m s−1, due to the decreased atmospheric transmission (by about 20 % on the two-way transmission). The effect of a cirrus cloud on wind and backscatter coefficient retrieval accuracies at different levels is discussed in Sect. 4.5 as a function of the cirrus optical thickness.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f08

Figure 8Vertical profile of the horizontal wind speed error (standard deviation) for different backscatter profiles, i.e., LQ, MD, HQ, and MD plus cirrus for the optimal parameters Δ=3.2 cm and θ=45. (a) Constant vertical resolution of 0.5 km. (b) Variable vertical resolution (0.5 to 2 km) and requirements, according to Aeolus.

Download

Table 3HLOS wind statistical error of the proposed QMZ design compared to the original Aeolus requirements.

Download Print Version | Download XLSX

4.4 Backscatter measurements

The choice of a small OPD is a strong advantage for wind measurements in clear air but is not optimized for retrieving the particulate backscatter coefficient (the OPD should be larger as discussed before; see also BP03). The QMZ technique with the selected parameters can, nevertheless, retrieve backscatter coefficients and determine the lidar scattering ratio Rβ (see Appendix A) with a relatively good accuracy, as we will see now. The derivation of the particulate backscatter requires the knowledge of the molecular backscatter coefficient βmol and the calculation of the molecular and particle interference modulations Mmol and Mpar, respectively. These calculations necessarily bring additional errors in the backscatter retrieval process. They are summarized later in this section and detailed in Appendix D.

Let us first look to noise-induced errors, assuming no other random error source. Figure 9 shows the relative standard deviation of the statistical error on Rβ and on βpar (according to Eqs. A18 and A19 in Appendix A) for the LQ, MD, HQ, and MD with cirrus backscatter profiles.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f09

Figure 9Actual scattering ratio. (a) Relative statistical error (standard deviation) on the scattering ratio measurement, (b) on the backscatter coefficient, (c) and on the extinction coefficient (d) for LQ, MD, HQ, and MD plus cirrus backscatter profiles.

Download

The scattering ratio Rβ can be retrieved with a relative statistical error of approximately 1 % over the troposphere, except above the tropical tropopause and in the first kilometer above the surface, where the error can increase up to 10 % due to the strong atmospheric attenuation for the HQ aerosol distribution. It can be argued that, in this case, the scattering ratio corresponds to a more polluted situation (Rβ∼3), where such a reduced precision may be more acceptable than an equivalent bias for assimilation purposes (Ma et al., 2019).

The error on αpar is somehow more important than for βpar due to the simple linear signal derivative procedure used in this analysis. More suitable and more efficient methods can be applied by distinguishing, slicing, and processing aerosol sublayers one by one, taking advantage of the simultaneous retrieval of backscatter and transmission and further extending previous analyses (Young, 1995; Young and Vaughan, 2009) and possibly using variational methods. This is, however, beyond the scope of this paper. Nevertheless, as seen in Fig. 9d, using this simple derivative method, the relative error remains smaller than 10 % in the boundary layer.

Let us now look at the errors due to the use of meteorological re-analyses for the retrieval of the particulate backscatter. These errors, often qualified as random systematic, are inherent to the modeling of the molecular scattering, which depends on the temperature profile using an a priori guess and including random errors. They are for the most part common to all the retrieval processes, whatever the measurement method. The particle backscatter and extinction retrieval (Eqs. A8–A10) requires knowledge of βmol and Mmol. The calculation of Mmol is not as straightforward as that given by Eq. (A14), since it must include the effect of Brillouin scattering. For an operating wavelength of 355 nm, the Brillouin doublet separation is much smaller than the thermal linewidth. The resulting spectrum is a broadening and distortion of the Gaussian profile. A correction can be derived from a model (Tenti et al., 1974) or measurements (Witschas et al., 2010). The effect is to the first-order proportional to the pressure with a maximum relative broadening of 1.7 % near the ground. This broadening causes a relative decrease in Mmol of 6×10-3, as compared to that calculated from the Gaussian thermal line. The Brillouin effect must be included in the calculation of Mmol, but the uncertainty on the actual atmospheric pressure leads to a second-order variation that can be neglected. This constraint is less critical here for the quantification of the molecular backscatter coefficient than for wind measurements using a DE-FP device (Dabas et al., 2008).

As seen in Appendix A (Eqs. A14 and A15), Mmol is sensitive to temperature, and this effect may significantly contribute in clear air and must be taken into account. The molecular linewidth γmol varies as the square root of temperature (see Eq. A15), which leads to a variation of about 20 % over the atmospheric column for a standard temperature profile. Assuming that the atmospheric temperature is known from a meteorological model to within 2 K allows the reduction of the uncertainty on Mmol to less than 0.5 % (see Appendix D; Fig. D2a). The other source of error on the particle backscatter coefficient comes from the modeling of the molecular backscatter coefficients, which is proportional to the molecular density and then also depends on the temperature vertical profile. As a whole, the knowledge of atmospheric temperature to within 2 K allows the reduction of the relative uncertainty on βmol to less than 1 % (see Appendix D; Fig. D2b).

Note that wind speed variation or turbulence in the probed volume could slightly reduce Mpar; however, with a Doppler shift of 5.6 MHz per meter per second, the broadening of the particle-backscattered spectrum is much less than the emitted laser linewidth of 100–200 MHz, and thus, the impact on Mpar is negligible. We, therefore, consider that Mpar is not affected by the atmospheric conditions.

In clear air, the uncertainty on Mmol dominates the total error on the backscatter and extinction coefficients (see Appendix D; Eqs. D1 and D2), but in regions where the aerosol load is significant (Rβ≥2), contributions to the total error from uncertainty in βmol and Mmol remain small and comparable in magnitude. Figure 10 shows the relative errors on βpar and αpar given by a random temperature error σ(T)=2 K at all altitudes, computed for the MD plus CIR (cirrus) aerosol profile and a standard temperature profile. These errors must be root square summed (RSS) with the statistical errors caused by detection noise. The total relative error on βpar remains of the order of 1 % in the regions where the aerosol load is significant (Rβ≥2). The total relative error on αpar is largely dominated by the SNR random error and stays of the order of 10 % in the PBL.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f10

Figure 10Relative standard deviation on βpar (a) and on αpar (b) for the MD plus CIR backscatter coefficient distribution caused by uncertainties of 2 K in the atmospheric analysis as a function of altitude.

Download

4.5 Measurements in presence of semi-transparent clouds

The evolution of the measurement performance is modeled for the RMA-MD scattering profile with the addition of a semi-transparent (cirrus) cloud, whose optical thickness varies from 0 to 0.5. Figure 11 shows the SNR, errors in HLOS wind, backscatter, and extinction coefficients at different levels. The measurements above the cloud are almost unaffected, despite the increase in the background noise due to the increasing cloud albedo. Performance in the PBL below the cloud is degraded by the lower atmospheric transmission, while performance in the cloud is improved due to the higher return signal.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f11

Figure 11(a) SNR, (b) HLOS wind speed error, (c) βpar relative error, and (d) αpar relative error as a function of the cirrus vertical optical depth for different measurement altitudes.

Download

4.6 Instrument calibration dependent errors

The maximal value of the LOS velocity error and the relative error on the scattering ratio measurement are presented on Fig. 12, for a 10−3 relative error in the sensitivity calibration of a single QMZ channel, as a function of the scattering ratio and for LOS wind speeds extending from 0 to 100 m s−1.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f12

Figure 12Maximum measurement bias for a 10−3 relative calibration error in the sensitivity ai of one QMZ channel, as a function of the scattering ratio. (a) LOS velocity error. (b) Scattering ratio relative error for different LOS velocities (VLOS).

Download

The sensitivity parameters ai and modulation parameters Mi are determined by the calibration sequence presented in Sect. 3.5. As tested on the HSRD-LNG QMZ, fits of the recorded signals with the model described by Eq. (1) are obtained with a correlation better than 99.5 % (Bruneau et al., 2015; see also Appendix C). This allows the determination of the ai and Mi parameters with a high accuracy.

5 Discussion

From the parameters reported in Table 2 and the results presented in the previous section, the performance in the determination of the HLOS wind speed can be optimized using a single, compact QMZ. This MZI design offers a high-value alternative to the whole cascade FP-DE and Fizeau interferometric system implemented in the present Aeolus design. A better overall performance is expected to be achieved based on realistic parameters derived from airborne operation with a minimized risk and increased design compactness and reliability. As compared to the 35 LOS angle of Aeolus, a higher 45 slant viewing allows us to increase the LOS horizontal projection and also to obtain the same vertical resolution with a larger range gate and, hence, collected signal, slightly increasing the performance despite a lower atmospheric transmission and larger range.

The expression of errors has been compared to observations (see Appendix C), confirming the pertinence of the numerical model used. As can be seen from Table 3, the simulated performance is better than the original requirement for ADM-Aeolus in the lower stratosphere and free troposphere (even keeping a 1000 and 500 m resolution, respectively; see Fig. 8) and slightly worse in the boundary layer for a varying vertical resolution. This does not appear critical as meteorological stations are providing measurements at the surface, and there are spaceborne scatterometers over ocean. The achievable performance still appears to be acceptable and does not justify the introduction of a second interferometer optimized for particulate scattering, which would significantly complicate the instrument.

Aeolus has been studied to be operated with a 130 mJ/100 Hz transmitter to meet the requirements, but the development of the operational system only allowed the use of a 65 mJ/50 Hz transmitter. Considering equations of errors with SNR depending on the square root of the emitted power (product of energy and repetition rate) at high SNR, the reduction in the horizontal resolution (90 km instead of 50 km), and the change in altitude (320 km instead of 395/425 km), ALADIN in space should produce a statistical error increased by a factor of about 3.5, compared to its original dimensioning. The actual standard deviation of the Aeolus measurements achieved is about 4 m s−1 with the Rayleigh channel in the free troposphere and about 2 to 3 m s−1 with the Mie channel in the lower 2 km, both for a 90 km horizontal resolution (Reitebuch et al., 2020; Geiss et al., 2019; Witschas et al., 2020; Martin et al., 2021). In the troposphere, the actual Aeolus performance appears to be degraded by transmission losses by a factor 1.5 to 2 with respect to simulations (Reitebuch et al., 2020). This is mostly due to the narrow field of view requiring a high pointing accuracy due to the low DE-FP acceptance angle. The proposed field-compensated QMZ design offers more flexibility, and its actual performance is expected to be closer to the simulations.

As presented in Sect. 4.6, an instrument calibration error in the sensitivity ai on one channel by 10−3 propagates to wind measurements with a maximum LOS velocity error of 0.15 m s−1 (0.2 m s−1 in HLOS), depending on the interference phase (the bias averaged on all phases is negligible). This can appear relatively sensitive, but in fact, the calibration process given in Sect. 3.5 has been validated with the HSRD-LNG airborne system and indeed allows such a calibration accuracy. Actually, the average 0.12 m s−1 LOS wind speed bias observed with this system on a long series of ground returns (Bruneau et al., 2015) shows that the residual-phase-dependent bias is very limited. To monitor system health and avoid degradation of performance with time due to the aging of optical components, the calibration operation should nevertheless be done regularly. Note also that the high sensitivity of the wind speed measurement with regard to the instrument calibration is inherent to the spectral discrimination based on molecular scattering because of its large spectral distribution. For comparison, the characteristics of the DE-FP used at the Observatoire de Haute Provence (Souprayen et al., 1999b) led to a bias of 0.38 m s−1 in the LOS velocity measurement for a 10−3 sensitivity error on one channel. The actual ALADIN HLOS wind velocity measurement bias has been estimated to be around 1.5 m s−1, with a latitude- and orbit-phase dependence (Martin et al., 2021).

The wind measurement accuracy in presence of a cirrus cloud of variable optical depth, as frequently observed in the atmosphere, is not degraded so much for low cloud optical depths (Fig. 12b). HLOS wind speed errors are maintained below 3 and 5 m s−1 at altitudes of 1 km (top of the atmospheric boundary layer) and 5 km, respectively, in the presence of cirrus clouds with optical depths up to 0.5. Measurement errors in cirrus clouds remain low, allowing higher horizontal resolutions, which are highly valuable as they are close to the upper tropospheric jet.

Unlike the FPI-based HSRL technique proposed for ATLID, the QMZ technique does not attempt to directly separate molecular and particulate signals but delivers, in addition to the total signal Stot, the atmospheric interference modulation Matm from which the scattering ratio Rβ is derived (see Appendix A). The performance of the QMZ in terms of backscatter coefficient measurements is thus expressed differently than from those given by the EarthCare instrument. A determination of the particulate component of the signal is, however, possible by using molecular backscatter profiles from a model in Eq. (A11), introducing small additional errors (see the previous section and Appendix D). The retrieval of extinction can then be done in a very similar way as for conventional HSRL. We, nevertheless, can see (Fig. 9b) that the scattering ratio random error of 1 % in cirrus clouds with scattering ratios larger than 5 (with 500 m vertical and 50 km horizontal resolutions), as it is the case for most semi-transparent cirrus clouds, compares favorably with the radiometric errors of 50 % and 15 % for particulate and molecular signals, respectively, required for EarthCare (for 100 m/300 m vertical and 10 km horizontal resolutions; Hélière et al., 2012). Starting from the scattering ratio (and from separated molecular and particulate signals), it is further necessary to use an atmospheric model to derive the particulate backscatter and extinction coefficients (Eqs. A12 and A13). An error of about 2 K in the temperature leads to an error smaller than 1 % for both βpar and αpar in the PBL. These errors account for the molecular density, as for conventional HSRL, and for the Mmol temperature dependence, which can be seen as the equivalent of the temperature dependence of the transmission of the molecular channel in conventional technique. The QMZ performance simulations have been conducted with a vertical resolution derived from the Aeolus requirements and A-CCD characteristics taken from the ALADIN design. New A-CCDs with shorter time gates than those planned for ATLID would result in a higher vertical resolution compatible with the EarthCare requirements. Nevertheless, as the proposed configuration is aiming as a first priority to collect high-performance wind measurements, it is first requested to keep a low read noise per range gate as compared to the useful signal. Reducing the range gate duration thus implies a simultaneous reduction in read noise to keep an accuracy pertinent to the survey of dynamics and cloud parameters at the global scale.

In addition, the QMZ measurement is performed with a reference taken from the emitted pulse and does not require any frequency locking of the laser or the interferometer. The instrument is also tolerant to transmitter frequency linewidth, jitter (200 MHz RMS during half a second, included in the performance simulations), and is unaffected by long-term frequency drifts. The unfolded measurement range is ±832 m s−1, accepting the maximal earth rotational speed of 463 m s−1 without the need for a latitude-dependent LOS correction.

The design includes a relatively wide field angle (100 µrd; about 5 times larger than that of ALADIN and similar to the ATLID and CALIOP instruments), which relaxes the requirements on the transmitter–receiver alignment. This wider aperture angle also allows an increase in the emission cone and, thus, a reduction in the energy density at the surface, potentially also allowing the emission of other wavelengths in eye safety conditions. The solar background is, however, kept at the same level due a more severe interference filtering.

6 Conclusion

The Aeolus mission has emphasized new capabilities of lidar in space for wind measurements. The discussion of the Aeolus follow-on program allows us to revisit some of the choices made that have revealed technical constraints which limit achievable performance. In this paper, we explore possible solutions to relax some of the constraints identified, while retaining the initial performance objectives. A new spaceborne lidar design for horizontal wind speed measurement using a single QMZ interferometer technique is proposed for consideration for operational missions following Aeolus and EarthCare, taking advantage of advances made for both of them. The changes in the payload are minimized as the lidar system would use the same telescope aperture as Aeolus and a comparable 355 nm transmitter. A single quadri-channel Mach–Zehnder interferometer (QMZ) is selected to replace the cascade double-edge Fabry–Pérot (DE-FP) and Fizeau interferometers. The design of the QMZ can provide robustness and compactness and can be developed with molecular adherence as for Aeolus interferometers. The QMZ offers a large acceptance angle, reducing mechanical and thermal constraints. These choices allow us to overcome the limitations induced by the need of a narrow field of view for the DE-FP and the use of a high-accuracy alignment control and/or a drastic reduction in thermo-mechanical constraints. The QMZ design also relaxes constraints on the telescope focusing. There is no bias induced by aerosol scattering on Doppler shift, which also represents a strong advantage for the needed bias corrections in the assimilation process. The instrument is optimized for wind measurements over the whole troposphere as for Aeolus. It also authorizes the retrieval of cloud and aerosol optical properties with a satisfying accuracy as compared to the EarthCare mission. It further allows the implementation of a depolarization channel as for ATLID and HSRD-LNG, without degrading the overall performance and offering unbiased operation. For the retrieval of aerosol and cloud backscatter properties, the necessary knowledge of the molecular spectrum (including Brillouin scattering) can be derived from meteorological analyses to provide products with the required accuracy.

The performance study shows that a statistical error on the horizontal wind speed better than 2 m s−1 can be achieved, from the boundary layer up to the tropopause for a 500 m vertical resolution and a 50 km horizontal resolution. Accordingly, the measurement bias can be as small as 0.2 m s−1, provided a proper calibration is done. In addition to wind speed, the instrument can retrieve the scattering ratio with a relative random error of 1 % to 2 % over most of the troposphere, which is well matched to high cloud study and radiatively significant aerosol load. The performance analysis on the QMZ interferometer is supported by the overall performance of the UV HSRD-LNG airborne lidar developed and operated by LATMOS and Institute for Earth Sciences and Astronomy (INSU).

Appendix A: Signal processing and noise-dependent measurement errors

A1 Signal processing

In this appendix, we refer to BP03 to recall expressions of errors of atmospheric wind speed and attenuated backscatter coefficients using a QMZ interferometer. Let us start with the optical lidar signal Satm (in number of photons) at the QMZ input as follows:

(A1) S atm ( R ) = S mol ( R ) + S par ( R ) = E A T inst h ν r = R - δ R / 2 r = R + δ R / 2 ( β mol ( r ) + β par ( r ) ) r 2 T atm 2 ( r ) d r ,

where E is the emitted energy, A is the telescope area, Tinst is the instrumental (emission and reception) transmission, hν is the emission photon energy, R is the range, and Tatm(r)=exp-0rαmol(r)+αpar(r)dr and the mol and par subscripts are related to the molecular and particulate scattering respectively.

The signal delivered by each channel of the A-CCD outputs (in photoelectrons), for i=1 to 4, can be written as follows:

(A2) S i = S tot 4 a i 1 + M i M atm sin φ + ( i - 1 ) π 2 + S b , i .

ai is the relative photometric efficiency of channel i with i=14ai=4, and Mi is the intrinsic modulation of channel i. Sb,i is the background signal due to solar detected light and A-CCD intrinsic noise.

As all the photons incident on the MZI arrive on the detectors, we have the following:

(A3) S tot = 4 i = 1 4 M i - 1 i = 1 4 S i - S b , i a i M i = η S atm ,

where η is the mean quantum efficiency of the detectors.

φ is the interference phase, and Matm is the atmospheric effective interference modulation given by the molecular and particulate atmospheric backscattered signals as follows:

(A4) M atm = M par R β - 1 + M mol R β ,

where the lidar scattering ratio Rβ is defined by the ratio of the total to the molecular backscatter coefficients as Rβ=βmol+βparβmol.

Depending on the scattering ratio, the atmospheric modulation coefficient Matm varies between Mmol and Mpar, which is the interference modulations given by pure molecular and particulate signals, respectively.

After subtraction of the background, the four signals are combined two-by-two in order to produce a complex signal Q (with in-phase and quadrature components) as follows:

(A5) Q = Q 2 + i Q 1 with Q 1 = a 3 S 1 - S b 1 - a 1 S 3 - S b 3 a 3 M 3 S 1 - S b 1 + a 1 M 1 S 3 - S b 3 ; Q 2 = a 4 S 2 - S b 2 - a 2 S 4 - S b 4 a 4 M 4 S 2 - S b 2 + a 2 M 2 S 4 - S b 4 .

The interference phase, φ, is obtained by the argument of the complex signal Q as follows:

(A6) φ = arg ( Q ) .

Subtracting the reference phase φr, obtained in the same way on a highly attenuated pick-up of the laser emission, one can obtain the line-of-sight (LOS) particle velocity VLOS with the following:

(A7) V LOS = c λ 4 π Δ ( φ - φ r ) ,

where Δ is the MZI optical path difference, λ is the operating wavelength, and c is the light celerity both in vacuum. Using this differential approach, VLOS can be obtained on the whole measurement range ±cλ4Δ without the need for locking the emitting frequency with the interference phase.

The atmospheric modulation is obtained by the modulus of Q divided by the modulus of the reference signal as follows:

(A8) M atm = Q Q r .

One can see, from Eq. (A3), that once Mmol and Mpar are determined, Matm gives access to the scattering ratio Rβ.

(A9) R β = M par - M mol M par - M atm .

Separated molecular and particulate signals can be obtained (with the same instrumental constant) using the following:

(A10) S mol = M par - M atm M par - M mol S tot η ; S par = M atm - M mol M par - M mol S tot η ,

but this step is not necessary for the retrieval of the particulate backscatter and extinction coefficients which can be obtained as follows:

(A11) β par = β mol R β - 1 = β mol M atm - M mol M par - M atm .

The total particulate optical depth over the vertical column can be derived from the total signal and the scattering ratio as follows:

(A12) τ par = 1 2 ln R β β mol r 2 S tot - τ mol .

One way to determine the particulate extinction coefficient is to derive Eq. (A12) which gives the particulate optical depth with altitude z as follows:

(A13) α par = 1 2 d d r L n R β β mol r 2 S tot - α mol ,

which allows us to remove the need for calibration. This method is sensitive to noise, and other ways to derive extinction can provide better results. We will, however, use this conservative approach for the sake of simplicity.

A2 Preliminary evaluation of Mpar and Mmol

Assuming Gaussian spectral profiles, the two interference modulations Mmol and Mpar can be expressed as a function of the optical path difference Δ and the 1/e linewidth γ (expressed in wavenumber) of the related spectral functions of atmospheric scattering convolved by the laser emitted width, as given in BP03, so that, in the following:

(A14) M s = exp - π γ s Δ 2 ,

where s stands for mol or par. For the particle scattering, γpar is defined as a first approximation by the laser source linewidth γlas. Assuming γlas of the order of 3×10-3 cm−1 (or 100 MHz, corresponding to the transform limit of a 3 ns pulse), we see that we obtain γparΔ10-2 and Mpar≈1 for an OPD value of 3 cm. We, thus, remain in the case of a high contrast for the particulate signal, with some margin on the laser linewidth.

For the molecular scattering, γmol is dominated by the thermal molecular velocity as follows:

(A15) γ mol = 2 λ c 2 k T m ,

and is about 7×10-2 cm−1, which implies that γmolΔ0.2 and Mmol≈0.6 for an OPD of 3 cm.

A3 Noise-dependent statistical error

We give here the random error depending on the detected noise. Assuming, for simplicity, that all the relative sensitivities ai are equal to 1 and that all the instrumental modulations Mi are equal to M0, the standard deviation of VLOS is given in BP03 as follows:

(A16) σ V LOS = c λ 4 π Δ 2 SNR M 0 M atm 1 - 1 2 F B M 0 2 M atm 2 sin 2 ( 2 φ ) ,

where SNR is the signal-to-noise ratio, and FB is a correlation coefficient between the four detection channels given by FB=Stot-SbStot+Sb, where Stot is the number of signal photo-electrons, and Sb is the total number of photo-electrons of the radiative and detection background (both summed with the weighting factors given in Eq. A3). We also assume here that the background can be measured over an extended range gate and subtracted for any measurement pixel with a negligible impact on bias and SNR. This assumes that the background noise is taken with a much higher SNR than the atmospheric signal. For accurate measurements, the SNR needs to be high, so we have StotSb and FB≈1 leading to a minimum square root factor.

If, as we propose, the laser frequency is not locked to the interferometer, the phase can take any value between 0 and 2π. For the performance assessment of the instrument, we, thus, average the error on φ and obtain the following:

(A17) σ V LOS = c λ 4 π Δ 2 SNR 1 M 0 M atm 1 - M 0 2 M atm 2 4 .

The factor Dc=1M0Matm1-M02Matm24 can be seen as a degradation factor on the wind error due to the contrasting degradation. For high scattering ratios, we have MatmMpar1, and assuming a perfect MZI, we have M0∼1, so that Dc=1. In clear air, for which we have MatmMmol0.6, the degradation factor is Dc=1.6. This is intrinsic to the QMZ technique, for which error is reduced in presence of particle scattering.

The relative standard deviation of the statistical error on Rβ is linked to the error on modulus of Q (Eq. A8). After averaging over φ, it can be expressed as follows (BP03):

(A18) σ R β R β = 2 SNR R β M 0 M par - M mol 1 - 3 4 F B M 0 2 M atm 2 .

We can then derive the error on βpar as follows:

(A19) σ β par = 2 SNR R β β par + β mol M 0 M par - M mol 1 - 3 4 F B M 0 2 M atm 2 .

The error on the particulate extinction coefficient is given (after averaging over φ) by the following (BP03):

(A20) σ α par = 1 2 δ r 1 SNR 1 + 2 R β 2 M 0 2 M par - M mol 2 1 + 3 4 F B M 0 2 M atm 2 - R β M atm M par - M mol 1 + F B .
Appendix B: MZI field compensation and aperture

A MZI produces interferences between waves propagating in two arms, with one in a vacuum with the length L1, the other in a glass of optical index n and the length L2 (not taking into account the elements which are common to both arms). The OPD Δ between these two waves depends on the incidence angle i on the interferometer as follows:

(B1) Δ ( i ) = n L 2 cos ( r ) - L 1 cos ( i ) with sin ( i ) = n sin ( r ) .

After mathematical developments, we obtain the following:

(B2) Δ ( i ) = n L 2 - L 1 + 1 2 L 2 n - L 1 sin 2 ( i ) + 3 8 L 2 n 3 - L 1 sin 4 ( i ) + ε ,

where ε represents the terms of even order superior to 4 in sin (i).

The field compensation is obtained for L2=nL1, which cancels the term in sin 2(i). The remaining angle dependence can be written at the fourth order on i as follows:

(B3) Δ ( i ) = Δ 0 1 - 3 8 n 2 i 4 with Δ 0 = Δ ( i = 0 ) = n L 2 - L 1 ,

when averaged over the MZI aperture between 0 and imax, we have the following:

(B4) Δ = 2 i max 2 0 i max Δ ( i ) i d i = Δ 0 1 - i max 4 8 n 2 .

(B5) Δ 2 = 2 i max 2 0 i max Δ 2 ( i ) i d i = Δ 0 2 1 - i max 4 4 n 2 + 9 5 i max 8 2 6 n 4 .

The residual RMS wavefront error after field compensation is then as follows:

(B6) σ RMS = Δ 2 - Δ 2 = Δ 0 i max 4 4 5 n 2 .

As the beam étendue is maintained over its propagation through the instrument, the product of the useful interferometer aperture DMZI by the apparent source field angle αMZI is equal to the product of the receiving telescope apertureDtel by its field of view αtel. Besides, it can be shown that the minimal aperture DL for a beam propagating on a distance L with a specified Dtel by αtel product is DL=2DtelαtelL. As, for field compensation, the minimal optical propagation length in the MZI (both arms are equals) is Lmin=L1=Δ0n2-1. We can, therefore, consider that a realistic MZI (including all the elements common to the two arms) can be built with an internal propagation length of 0. The resulting useful diameter of the MZI is then as follows:

(B7) D MZI = 2 2 D tel α tel Δ 0 .

Then, for the instrumental parameters of this study, Dtel=1.5 m, αtel=0.1 mrd, OPD=3.2 cm, and the useful MZI aperture is DMZI=6.2 mm.

Using Eqs. (B6) and (B7) with imax=αMZI2=Dtelαtel2DMZI=Dtelαtel42Δ0, we obtain the following:

(B8) σ RMS = D tel 2 α tel 2 2 12 5 n 2 Δ 0 .

With our instrumental parameters, we find a residual wavefront distortion of σRMS=3.7×10-2 nm due to the field compensation.

Appendix C: Analysis of observed HSRD-LNG performance

C1 Wind measurements

In addition to the results presented in Bruneau et al. (2015), here we report wind measurements performed with HSRD-LNG aboard the SAFIRE Falcon 20 aircraft during the North Atlantic Waveguide and Downstream Impact Experiment and EarthCare PrepAraTion cAmpaigN (NAWDEX-EPATAN) field experiment (Schäfler et al., 2018) on 4 October 2016.

We remind the reader that, due to its OPD of 20 cm, the HSRD-LND interferometer is able to measure wind only from the particle scattering. The measurements were, therefore, performed in extended cirrus clouds from an altitude of 12 km, during 360 turns of the aircraft at a constant roll angle of 27, providing several LOS measurements at various levels in the cloud and allowing the performance of a velocity azimuth display (VAD) analysis at each level. For each VAD, the average wind module and direction is computed from a sine fit on approximately 100 LOS measurements of 100 shots each and extends on a circle of approximately 20 km in diameter for a total duration of 500 s. Figure C1a shows an example of measurements and VAD sine fit at an altitude of 7.9 km with a vertical resolution of 100 m.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f13

Figure C1(a) LOS wind speed retrieved by HSRD-LNG over 100 shots at an altitude of 7.9 km. (b) Comparison of the measured and calculated LOS wind speed (VLOS) errors.

Download

Taking the sine fit as a reference, we can compute the standard deviation of the LOS measurements and compare it to the standard deviation calculated with Eq. (A17). Figure C1b shows the comparison of the measured and calculated LOS wind speed standard deviations computed at different altitudes on three different VAD measurements taken at 16:37, 17:34 and 18:00 UTC (universal coordinated time; for a total of 98 measurements). Note that, because of the spatial and temporal extents of the VADs, the measured standard deviations include part of the natural variability and are, on average, slightly higher than the calculated standard deviations. Taking into account the natural variability, we can see that the measured and calculated errors are in good agreement, and we then consider that Eq. (A17) is validated.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f14

Figure C2HSRD-LNG VAD wind profiles (blue) with calculated error bars (standard deviation) and collocated radiosonde measurements (red) for NAWDEX-EPATAN VADs performed on 4 October 2016 for three dropsondes launched at (a) 16:30, (b) 17:30, and (c) 18:00 UTC. (d) Histogram of differences of HLOS wind speeds between HSRD-LNG, and related dropsonde measurements over the three vertical profiles.

Download

To further illustrate the capacity of the airborne HSRD-LNG to measure wind, Fig. C2a, b, and c present the three wind profiles retrieved from VADs analysis on 10 October 2016, compared to collocated radiosonde measurements. Figure C2d presents the histogram of the wind speed and wind direction differences between VAD lidar and dropsonde profiles. Table C1 summarizes the horizontal wind speed VHOR and wind direction VDIR differences between lidar and dropsonde profiles and the related standard deviations compared to the mean calculated standard deviations for the three cases of 10 October. As the lidar and dropsonde profiles cannot be perfectly collocated, the mean standard deviation of the profiles' difference includes the wind natural variability with different integrations in time and space, but the differences remain small.

Table C1Summary of mean differences between wind lidar and radiosonde profiles a, b, c, as given in Fig. C2, and related and related standard deviations (SDs).

Download Print Version | Download XLSX

C2 Particle backscatter coefficient measurements

To assess the measurement error on the particle backscatter coefficient, we compiled several ground-based measurements in the boundary layer. The raw βpar measurement variability includes both the instrumental error and the natural variability. In order to separate the two terms, we used a spectral analysis of the temporal series for each vertical range gate, as developed in Frehlich et al. (1998). The instrumental error is given by the plateau of the spectrum at high frequencies. These measured errors are compared to the calculated errors obtained from Eq. (A19) in Fig. C3. As measured and calculated errors are in fairly good agreement, we can consider that the error calculation used in the performance model for the backscatter coefficient is validated.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f15

Figure C3Comparison of the measured and calculated relative errors (standard deviation) on the particle backscatter coefficient.

Download

Appendix D: Atmosphere-modeling-dependent errors in the retrieval of particulate backscatter and extinction coefficients

As already pointed out, the wind speed measurement does not require any atmospheric modeling (unlike DE-FP operation), since the interference phase determination is independent of the actual interference modulation Matm. Nevertheless, the particle backscatter coefficient and extinction retrieval (Eqs. A8–A10) requires the knowledge of βmol. Mmol can be obtained with some atmosphere modeling and assumptions.

The calculation of Mmol is not as straightforward as that given by Eq. (A14), since it must include the effect of Brillouin scattering. For an operating wavelength of 355 nm, the Brillouin doublet separation is much smaller than the thermal linewidth. The resulting spectrum is a broadening and distortion of the Gaussian profile. A correction can be derived from a model (Tenti et al., 1974) or measurements (Witschas et al., 2010). The effect is roughly proportional to the pressure with a maximum relative broadening of 1.7 % near the ground. This broadening causes a relative decrease in Mmol of up to 6×10-3 compared to a Gaussian thermal line (Fig. C1). The Brillouin effect must be included in the calculation of Mmol, but the uncertainty on the actual atmospheric pressure leads to a second-order variation in Mmol that can be neglected. This constraint is less critical here for the quantification of the molecular backscatter coefficient than for wind measurements using a DE-FP device (Dabas et al., 2008).

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f16

Figure D1Reduction in Mmol caused by the Brillouin effect.

Download

In contrast, the dependence of Mmol on temperature, given in Fig. D2a for a standard profile, must be taken into account. The molecular linewidth γmol varies as the square root of temperature (see Eq. A15), which leads to a variation of about 20 % over the atmospheric column. The knowledge of atmospheric temperature to within 2 K allows the reduction of uncertainty on Mmol to less than 1 %.

The other source of error on the particle backscatter coefficient comes from the modeling of the molecular backscatter coefficients, which is proportional to the molecular density and then depends on the temperature vertical profile. The sensitivity of the relative error with regard to temperature is presented on Fig. D2b.

The relative error on the retrieval of the particle backscatter coefficient caused by atmospheric analysis errors is derived from Eq. (A11) as follows:

(D1) σ β par β par atm = [ d β mol β mol d T 2 + d M mol M par - M mol d T 1 R β - 1 2 - 2 M par - M mol R β - 1 d β mol β mol d T d M mol d T ] 1 2 σ ( T ) .

Considering Eq. (A13) and assuming that the temperature errors between range gates are independent and with the same standard deviation σ(T), we obtain, for the error on the particle extinction coefficient caused by the atmosphere modeling uncertainties, the following:

(D2) σ α par atm = [ cos θ 2 Δ z d β mol β mol d T 2 + cos θ 2 Δ z d M mol M par - M mol d T 2 - 2 M par - M mol cos θ 2 Δ z 2 d ( β mol ) β mol d T d ( M mol ) d T + 8 π 3 d ( β mol ) d T 2 ] 1 2 σ ( T ) ,

where Δz is the vertical resolution, and θ is the LOS nadir angle.

https://amt.copernicus.org/articles/14/4375/2021/amt-14-4375-2021-f17

Figure D2Temperature sensitivity for (a) Mmol and (b) βmol as a function of altitude.

Download

Code and data availability

Information on code and data are available on request to Didier Bruneau (didier.bruneau@latmos.ipsl.fr).

Author contributions

JP designed the paper and established the main issues. DB defined the instrumental design and established the performance modeling. Both authors participated in the writing of the paper.

Competing interests

The authors declare that they have no conflict of interest.

Special issue statement

This article is part of the special issue “Aeolus data and their application (AMT/ACP/WCD inter-journal SI)”. It is not associated with a conference.

Acknowledgements

The authors wish to acknowledge CNES for their support in developing the airborne instrument HSRD-LNG and in related field experiments. ESA is also acknowledged for their support in the NAWDEX-EPATAN field experiment in 2016. The authors would like to warmly thank all their colleagues from LATMOS and INSU-DT for their contributions which made the HSRD-LNG project a reality.

The two anonymous reviewers are acknowledged for their comments and suggestions that led to the improvement of this paper.

This paper is dedicated to the memory of our colleague Pierre H. Flamant, a major actor in the development of wind lidar. He passed away at the end of June 2020. He was the president of the early Aeolus Mission Advisory Group at ESA and contributed to several projects and field experiments, thereby paving the way in this new research area.

Review statement

This paper was edited by Oliver Reitebuch and reviewed by two anonymous referees.

References

ASAG: Aeolus Science Advisory Group recommendations for operational Doppler Wind Lidar (DWL) observation requirements in the 2030–2040 timeframe, v1.1, EOPSM-AEOL-TN-3695, 128 pp., 2020. 

Baker, W. E., Emmitt, G. D., Robertson, F., Atlas, R. M., Molinari, J. E., Bowdle, D. A., Peagle, J., Hardesty, R. M., Menzies, R. T., Krishnamurti, T. N., Brown, R. A., Post, M. J., Anderson, J. A., Lorenc, A. C., and McElroy, J. E.: Lidar-Measured winds from Space: A key component for weather and climate prediction, B. Am. Meteorol. Soc., 76, 869–888, 1995. 

Baker, W. E., Atlas, R., Cardinali, C., Clement, A., Emmitt, G. D., Gentry, B. M., Hardesty, R. M., Källén, E., Kavaya, M. J., Langland, R., Ma, Z., Masutani, M., McCarty, W., Pierce, R. B., Pu, Z., Riishojgaard, L P., Ryan, J., Tucker, S., Weissmann, M., and Yoe, J. G.: Lidar-Measured Wind Profiles: The Missing Link in the Global Observing System, B. Am. Meteorol. Soc., 95, 543–564, https://doi.org/10.1175/BAMS-D-12-00164.1, 2014. 

Bouchareine, P. and Connes, P., Interferometer with compensated field for Fourier transform spectroscopy, J. Phys. Rad., 24, 134–138, 1963. 

Bruneau, D.: Mach-Zehnder interferometer as a spectral analyzer for molecular Doppler wind lidar, Appl. Optics, 40, 391–399, 2001. 

Bruneau, D.: Fringe-imaging Mach-Zehnder interferometer as a spectral analyser for molecular Doppler wind lidar, Appl. Optics, 41, 503–510, 2002. 

Bruneau, D. and Pelon, J.: Simultaneous measurements of particle backscatter and extinction coefficients and wind velocity by lidar with a Mach–Zehnder interferometer: principle of operation and performance assessment, Appl. Optics, 42, 1101–1114, 2003. 

Bruneau, D., Garnier, A., Hertzog, A., and Porteneuve, J.: Wind-velocity lidar measurements by use of a Mach-Zehnder interferometer, comparison with a Fabry-Perot interferometer, Appl. Optics, 43, 173–182, 2004. 

Bruneau, D., Pelon, J., Blouzon, F., Spatazza, J., Genau, P., Buchholtz, G., Amarouche, N., Abchiche, A., and Aouji, O.: 355 nm high spectral resolution airborne lidar LNG: system description and first results, Appl. Optics, 54, 8776–8785, 2015. 

Burton, S. P., Ferrare, R. A., Hostetler, C. A., Hair, J. W., Rogers, R. R., Obland, M. D., Butler, C. F., Cook, A. L., Harper, D. B., and Froyd, K. D.: Aerosol classification using airborne High Spectral Resolution Lidar measurements – methodology and examples, Atmos. Meas. Tech., 5, 73–98, https://doi.org/10.5194/amt-5-73-2012, 2012. 

Cazenave, Q., Pelon, J., Delanoë, J., Collomb, H., and Blouzon, F.: Contribution to the CAL/VAL of the Aeolus mission using 355 nm HSR Doppler Lidar and 95 GHz Doppler cloud radar, Aeolus CAL/VAL workshop, March 26-29, 2019, Frascatti, 2019. 

Cézard, N., Dolfi-Bouteyre, A., Huignard, J.-P., and Flamant, P. H.: Performance evaluation of a dual fringe-imaging Michelson interferometer for air parameter measurements with a 355 nm Rayleigh-Mie lidar”, Appl. Optics, 48, 2321–2332, 2009. 

Chanin, M.-L., Garnier, A., Hauchecorne, A., and Porteneuve, J.: A Doppler LIDAR for measuring winds in the middle atmosphere, Geophys. Res. Let., 16, 1273–1276, 1989. 

Cheng, Z., Liu, D., Luo, J., Yang, Y., Zhou, Y., Zhang, Y., Duan, L., Su, L., Yang, L., Shen, Y., Wang, K., and Bai, J.: Field-widened Michelson Interferometer for spectral discrimination in high-spectral resolution lidar: theoretical framework, Opt. Express, 23, 12117–12134, 2015. 

Dabas, A., Denneulin, M., Flamant, P., Loth, C., Garnier, A., and Dolfi-Bouteyre, A.: Correcting winds measured with a Rayleigh Doppler lidar from pressure and temperature effects, Tellus A, 60, 206–215, 2008. 

Delanoë, J., Protat, A., Jourdan, O., Pelon, J., Papazzoni, M., Dupuy, R., Gayet, J., and Jouan, C.: Comparison of airborne in-situ, airborne radar-lidar, and spaceborne radar-lidar retrievals of polar ice cloud properties sampled during the POLARCAT campaign, J. Atmos. Ocean. Tech., 30, 57–73, https://doi.org/10.1175/JTECH-D-11-00200.1, 2012. 

Eloranta, E. W., Razenkov, I. A., Hedrick, J., and Garcia, J. P.: The Design and Construction of an Airborne High Spectral Resolution Lidar, in: 2008 IEEE Aerospace Conference, 1–8 March 2008, Big Sky, MT, 1–6, https://doi.org/10.1109/AERO.2008.4526390, 2008. 

ESA: The Four Candidate Earth Explorer Core Missions – Atmospheric Dynamics, edited by: Battrick, B., publication SP-1233 (4), 157 pp., ISBN 92-9092-528-0, 1999. 

ESA: Aeolus-ESA-Portal-mission, available at: https://earth.esa.int/web/eoportal/satellite-missions/a/adm-aeolus (last access: 1 June 2021), 2002. 

ESA: ADM-Aeolus science report, edited by: Clissold, P., European Space Agency, Rep. ESA SP-1311, 121 pp., 2008. 

ESA: Atmospheric Dynamics Mission, ADM-Aeolus, Mission Requirements Document, ESA, AE-RP-ESA-SY-001 EOP-SM/2047, Issue 2, 57 pp., 2016. 

ESA: Aeolus-ESA-Portal-forecast, available at: https://www.esa.int/Applications/Observing_the_Earth/Aeolus/Aeolus_winds_now_in_daily_weather_forecasts (last access: 1 June 2021), 2020. 

Esselborn, M., Wirth, M., Fix, A., Tesche, M., and Ehret, G.: Airborne high spectral resolution lidar for measuring aerosol extinction and backscatter coefficients, Appl. Optics, 47, 346–358, https://doi.org/10.1364/AO.47.000346, 2008. 

Flamant, P., Cuesta, J., Denneulin, M.-L., Dabas, A., and Huber D.: ADM-Aeolus retrieval algorithms for aerosol and cloud products, Tellus A, 60, 273–286, 2008. 

Frehlich, R., Hannon, S., and Henderson, S.: Coherent Doppler lidar measurements of wind field statistics, Bound.-Lay. Meteor., 86, 223–256, 1998. 

Garnier, A.: Etude, développement et premiers résultats d'un nouveau LIDAR Doppler destiné à la mesure des vents dans la moyenne atmosphère, PhD thesis, University Paris XI, Orsay, France, 1990 (in French). 

Garnier, A. and Chanin, M.-L.: Description of a Doppler Rayleigh lidar for measuring winds in the middle atmosphere, Appl. Phys. B, 55, 35–40, 1992. 

Geiss, A., Lehmann, V., Leinweber, R., Martin, A., and Weissmann, M.: Validation of Aeolus Observations by means of co-located reference measurements, in: Aeolus CAL.VAL & Science Workshop, Frascatti, 26–29 March 2019, ESA-ESRIN, 2019. 

Grund, C. J., Howell, J., Pierce, R., and Stephens, M.: Optical autocovariance direct detection lidar for simultaneous wind, aerosol, and chemistry profiling from ground, air, and space platforms, SPIE Defense & Security Sensing Symposium, conference on Advanced Environmental, Chemical, and Biological Sensing Technologies VI, Paper 7312-37, Orlando, Florida, United Sates, 2009. 

Hair, J. W., Hostetler, C. A., Cook, A. L., Harper, D. B., Ferrare, R. A., Mack, T. L., Welch, W., Izquierdo, L. R., and Hovis, F. E.: Airborne high-spectral-resolution lidar for profiling aerosol optical profiles, Appl. Optics, 47, 6734–6752, 2008. 

Hélière, A., Gelsthorpe, R., Le Hors, L., and Toulemont, Y.: ATLID, the atmospheric lidar on board the Earthcare Satellite, International Conference on Space Optics 2012 Proc. SPIE Vol 10564, ESA and CNES, Ajaccio, Corsica, France, 2012. 

Herbst, J. and Vrancken, P.: Design of a Monolithic Michelson interferometer for Fringe-Imaging in a Near-Field, UV, Direct Detection Doppler Wind Lidar, Appl. Optics, 55, 6910–6929, 2016. 

Illingworth, A. J., Barker, H. W., Beljaars, A., Ceccaldi, M., Chepfer, H., Clerbaux, N., Cole, J., Delanoë, J., Domenech, C., Donovan, D. P., Fukuda, S., Hirakata, M., Hogan, R. J., Huenerbein, A., Kollias, P., Kubota, T., Nakajima, T., Nakajima, T. Y., Nishizawa, T., Ohno, Y., Okamoto, H., Oki, R., Sato, K., Satoh, M., Shephard, M. W., Velázquez-Blázquez, A., Wandinger, U., Wehr, T., and van Zadelhoff, G. J.: The EarthCare satellite: The next step forward in global measurements of clouds, aerosols, precipitation, and radiation, B. Am. Meteorol. Soc., 96, 1311–1332, https://doi.org/10.1175/BAMS-D-12-00227.1, 2015. 

LAWS (Lidar Atmospheric Wind Sounder): Instrument Panel Report, NASA, Washington DC, vol. IIg, 55 p., 1987. 

Le Pichon, A., Assink, J. D., Heinrich, P., Blanc, E., Charlton-Perez, A., Lee, C. F., Keckhut, P., Hauchecorne, A., Rüfenacht, R., Kämpfer, N., Drob, D. P., Smets, P. S. M., Evers, L. G., Ceranna, L., Pilger, C., Ross, O., and Claud, C. “Comparison of co-located independent ground-based middle atmospheric wind and temperature measurements with numerical weather prediction models”, J. Geophys. Res. Atmos., 120, 8318–8331, https://doi.org/10.1002/2015JD023273, 2015. 

Liu, D., Hostetler, C., Miller, I., Cook, A., and Hair, J.: System analysis of a tilted field-widened Michelson interferometer for high spectral resolution lidar, Opt. Exp., 20, 1406–1420, 2012. 

Lux, O., Lemmerz, C., Weiler, F., Marksteiner, U., Witschas, B., Rahm, S., Geiß, A., and Reitebuch, O.: Intercomparison of wind observations from the European Space Agency's Aeolus satellite mission and the ALADIN Airborne Demonstrator, Atmos. Meas. Tech., 13, 2075–2097, https://doi.org/10.5194/amt-13-2075-2020, 2020. 

Ma, C., Wang, T., Jiang, Z., Wu, H., Zhao, M., Zhuang, B., Li, S., Xie, M., Li, M., Liu, J., and Wu, R.: Importance of bias correction in data assimilation of multiple observations over eastern China using WRF-Chem/DART, J. Geophys. Res.-Atmos., 125, e2019JD031465, https://doi.org/10.1029/2019JD031465, 2019. 

McCormick, M. P., Winker, D. M., Browell, E.V., Coakley, J. A., Gardner, C. S., Hoff, R. M., Kent, G. S., Melfi, S. H, Menzies, R. T., Platt, C. M., Randall, D. A., and Reagan, J. A.: Scientific Investigations Planned for the Lidar In-Space Technology Experiment (LITE), B. Am. Meteorol. Soc., 74, 205–214, https://doi.org/10.1175/1520-0477(1993)074<0205:SIPFTL>2.0.CO;2, 1993. 

Martin, A., Weissmann, M., Reitebuch, O., Rennie, M., Geiß, A., and Cress, A.: Validation of Aeolus winds using radiosonde observations and numerical weather prediction model equivalents, Atmos. Meas. Tech., 14, 2167–2183, https://doi.org/10.5194/amt-14-2167-2021, 2021. 

Mioche, G., Josset, D., Gayet, J.-F., Pelon, J., Garnier, A., Minikin, A., and Schwarzenboeck, A.: Validation of the CALIPSO/CALIOP extinction coefficients from in situ observations in mid-latitude cirrus clouds during CIRCLE-2 experiment, J. Geophys. Res., 115, D00H25, https://doi.org/10.1029/2009JD012376, 2010. 

Müller, D., Hostetler, C. A., Ferrare, R. A., Burton, S. P., Chemyakin, E., Kolgotin, A., Hair, J. W., Cook, A. L., Harper, D. B., Rogers, R. R., Hare, R. W., Cleckner, C. S., Obland, M. D., Tomlinson, J., Berg, L. K., and Schmid, B.: Airborne Multiwavelength High Spectral Resolution Lidar (HSRL-2) observations during TCAP 2012: vertical profiles of optical and microphysical properties of a smoke/urban haze plume over the northeastern coast of the US, Atmos. Meas. Tech., 7, 3487–3496, https://doi.org/10.5194/amt-7-3487-2014, 2014. 

National Academies of Sciences, Engineering, and Medicine: Thriving on Our Changing Planet: A Decadal Strategy for Earth Observation from Space, The National Academies Press, Washington, DC, https://doi.org/10.17226/24938, 2018. 

Paffrath, U.: Performance assessment of the Aeolus Doppler wind lidar prototype, D-Ing dissertation, Technische Universität München and DLR Forschungsbericht, Munich, 2006. 

Reitebuch, O., Lemmerz, C., Nagel, E., Paffrath, U., Durand, Y., Endemann, M., Fabre, F., and Chaloupy, M.: The airborne demonstrator for the direct-detection Doppler wind lidar ALADIN on ADM-Aeolus, 2009: I. Instrument design and comparison to satellite instrument, J. Atmos. Ocean. Tech., 26, 2501–2515, 2009. 

Reitebuch, O., Lemmerz, C., Mux, O., Markensteiner, U., Schmidt, K., Huber, D., Nicolaus, I., Dabas, A., Flament, T., Rennie, M., and Kanitz, T.: ALADIN's radiometric and frequency performance, Aeolus CAL.VAL & Science Workshop, Frascatti, ESA-ESRIN, 26–29 March 2019. 

Reitebuch, O., Lemmerz, C., Lux, O., Marksteiner, U., Rahm, S., Weiler, F., Witschas, B., Meringer, M., Schmidt, K., Huber, D., Nikolaus, I., Geiss, A., Vaughan, M., Dabas, A., Flament, T., Stieglitz, H., Isaksen, L., Rennie, M., de Kloe, J., Marseille, G.-J., Stoffelen, A., Wernham, D., Kanitz, T., Straume, A.-G., Fehr, T., von Bismarck, J., Floberghagen, R., and Parrinello, T.: Initial Assessment of the performance of the first wind lidar in space on Aeolus, ILRC29, EPJ Web Conf., 237, 01010, https://doi.org/10.1051/epjconf/202023701010, 2020. 

Rennie, M. and Isaksen, L.: Use of Aeolus observations at ECMWF, ECMWF Newsletter No. 163, 4–5, available at: https://www.ecmwf.int/en/elibrary/19508-newsletter-no-163-spring-2020 (last access: 31 May 2021), 2020. 

Schäfler, A., Craig, G., Wernli, H., Arbogast, P., Doyle, J. D., McTaggart-Cowan, R., Methven, J., Rivière, G., Ament, F., Boettcher, M., Bramberger, M., Cazenave, Q., Cotton, R., Crewell, S., Delanoë, J., Dörnbrack, A., Ewald, F., Fix, A., Gray, S. L., Grob, H., Groß, S., Hagen, M., Harvey, B., Hirsch, L., Jacob, M., Kölling, T., Konow, H., Lemmerz, C., Lux, O., Magnusson, L., Mayer, B., Mech, M., Moore, R., Pelon, J., Quinting, J., Rahm, S., Rapp, M., Rautenhaus, M., Reitebuch, O., Reynolds, C. A., Sodemann, H., Spengler, T., Vaughan, G., Wendisch, M., Wirth, M., Witschas, B., Wolf, K., and Zinner. T., The North Atlantic Waveguide and Downstream Impact Experiment, B. Am. Meteorol. Soc., 99, 1607–1637, 2018. 

Shipley, S. T., Tracy, D. H., Eloranta, E. W., Trauger, J. T., Sroga, J. T., Roesler, F. L., and Weinman, J. A.: High spectral resolution lidar to measure optical scattering properties of atmospheric aerosols. 1: Theory and instrumentation, Appl. Optics, 22, 3716–3724, 1983. 

Smith, J. A and Chu, X.: Investigation of a field-widened Mach–Zehnder receiver to extend Fe Doppler lidar wind measurements from the thermosphere to the ground, Appl. Optics, 55, 1366–1380, https://doi.org/10.1364/AO.55.001366, 2016. 

Souprayen, C., Garnier, A., Hertzog, A., Hauchecorne, A., and Porteneuve, J., Rayleigh-Mie Doppler wind lidar for stratospheric measurements, I. Instrumental setup, validation and first climatological results, Appl. Optics, 38, 2410–2421, 1999a. 

Souprayen, C., Garnier, A., and Hertzog, A.: Rayleigh-Mie Doppler wind lidar for stratospheric measurements II: Impact of Mie scattering, theory and calibration, Appl. Optics, 38, 2422–2431, 1999b. 

Sroga, J. T., Eloranta, E. W., Shipley, S. T., Roesler, F. L., and Tryon, P. J.: High spectral resolution lidar to measure optical scattering properties of atmospheric aerosols. 2: Calibration and data analysis, Appl. Optics, 22, 3725–3732, 1983. 

Stephens G., Winker, D., Pelon, J., Trepte, C., Vane, D., Yuhas, C., L'Ecuyer, T., and Lebsock, M.: CloudSat and CALIPSO within the A-Train: Ten years of actively observing the Earth system, B. Am. Meteorol. Soc., 99, 569–581, https://doi.org/10.1175/BAMS-D-16-0324.1, 2018. 

Stephens, G. L., Vane, D. G., Boain, R. J., Mace, G. G., Sassen, K., Wang, Z., Illingworth, A. J., O'Connor, E. J., Rossow, W. B., Durden, S. L., Miller, S. D., Austin, R. T., Benedetti, A., Mitriscu, C., and the CloudSat Team: The CloudSat mission and the A-train: A new dimension of spacebased observations of clouds and precipitation, B. Am. Meteorol. Soc., 83, 1771–1790, https://doi.org/10.1175/BAMS-83-12-1771, 2002. 

Stoffelen, A., Pailleux, J., Källen, E., Vaughan, J. M., Isaksen, L., Flamant, P., Wergen, W., Andersson, E., Schyberg, H., Culoma, A., Meynart, R., Endemann, M., and Ingmann, P., The Atmospheric Dynamics Mission for global wind field measurement, B. Am. Meteorol. Soc., 86, 73–88, https://doi.org/10.1175/BAMS-D-16-0324.1, 2005. 

Stoffelen, A., Benedetti, A., Borde, R., Dabas, A., Flamant, P., Forsythe, M., Hardesty, M., Isaksen, L., Källén, E., Körnich, H., Lee, T., Reitebuch, O., Rennie, M., Riishøjgaard, L.-P., Schyberg, H., Straume A. G., and Vaughan, M.: Wind profile satellite observation requirements and capabilities, B. Am. Meteorol. Soc., 101, 2005–2021, https://doi.org/10.1175/BAMS-D-18-0202.1, 2020. 

Tenti, G., Boley, C., and Desai, R.: On the kinetic model description of Rayleigh-Brillouin scattering from molecular gases, Can. J. Phys., 52, 285–290, 1974. 

Tucker, S., Walters, B., Applegate, J., and Springer, C.: The Nested-OAWL approach to full tropospheric wind measurements: building on Aeolus and CALIPSO for future operational wind missions, Aeolus CAL.VAL & Science Workshop, Frascatti, ESA-ESRIN, 26–29 March 2019. 

Tucker, S., Walters, B., Applegate, J., and Springer, C.: The Nested-OAWL approach to full tropospheric wind measurements: building on Aeolus and CALIPSO for future operational wind missions, Aeolus CAL.VAL & Science Workshop, Frascatti, ESA-ESRIN, 2–6 November 2020. 

Tucker, S. C., Weimer, C. S., Baidar, S., and Hardesty, R. M.: The Optical Autocovariance Wind Lidar. Part I: OAWL Instrument Development and Demonstration, J. Atmos. Ocean. Tech., 35, 2079–2097, https://doi.org/10.1175/JTECH-D-18-0024.1, 2018. 

Vaughan, J. M., Geddes, N. J., Flamant, P. H., and Flesia C.: Establishment of a backscatter coefficient and atmospheric database, ESA contract 12510/97/NL/RE, 110 pp., 1998. 

Weiler, F., Kanitz, T., Huber, D., and Reitebuch, O.: Aeolus dark current and hot pixels, Aeolus CAL.VAL & Science Workshop, Frascatti, ESA-ESRIN, 26–29 March 2019. 

Winker, D. M., Pelon, J., Coakley Jr., J. A., Ackerman, S. A., Charlson, R. J., Colarco, P. R., Flamant P., Fu, Q., Hoff, R. M., Kittaka, C., Kubar, T. L., Le Treut H., McCormick, P., Mégie, G., Poole, L., Powell, K., Trepte, C., Vaughan, M. A., and Wielicki, B. A.: The CALIPSO Mission: A global 3D view of aerosols and clouds, B. Am. Meteorol. Soc., 91, 1211–1229, https://doi.org/10.1175/2010BAMS3009.1, 2010. 

Witschas, B., Vieitez, M. O., van Duijn, E.-J., Reitebuch, O., van de Water, W., and Ubachs, W.: Spontaneous Rayleigh–Brillouin scattering of ultraviolet light in nitrogen, dry air, and moist air, Appl. Optics, 49, 4217–4227, 2010. 

Witschas, B., Lemmerz, C., Geiß, A., Lux, O., Marksteiner, U., Rahm, S., Reitebuch, O., and Weiler, F.: First validation of Aeolus wind observations by airborne Doppler wind lidar measurements, Atmos. Meas. Tech., 13, 2381–2396, https://doi.org/10.5194/amt-13-2381-2020, 2020. 

WMO: Guide to meteorological instruments and methods of observation, 6th edn., WMO-8, 681 pp., 1996. 

WMO: WIGOS: WMO Integrated Global Observing System; Final report of the Fifth WMO Workshop on the Impact of Various Observing Systems on Numerical Weather Prediction, WMO Tech. Rep. 2012-1, 23 pp., 2012.  

Young, S. A.,: Lidar analysis of lidar backscatter profiles in optically thin clouds, Appl. Optics, 34, 7019–7031, 1995. 

Young, S. A. and Vaughan, M. A.: The retrieval of profiles of particulate extinction from Cloud Aerosol Lidar Infrared Pathfinder Satellite Observations (CALIPSO) data: Algorithm description, J. Atmos. Ocean. Tech., 26, 1105–1119, https://doi.org/10.1175/2008JTECHA1221.1, 2009. 

Zhai, X., Marksteiner, U., Weiler, F., Lemmerz, C., Lux, O., Witschas, B., and Reitebuch, O.: Rayleigh wind retrieval for the ALADIN airborne demonstrator of the Aeolus mission using simulated response calibration, Atmos. Meas. Tech., 13, 445–465, https://doi.org/10.5194/amt-13-445-2020, 2020. 

Download
Short summary
Taking advantage of Aeolus success and of our airborne lidar system expertise, we present a new spaceborne wind lidar design for operational Aeolus follow-on missions, keeping most of the initial lidar system but relying on a single Mach–Zehnder interferometer to relax operational constraints and reduce measurement bias. System parameters are optimized. Random and systematic errors are shown to be compliant with the initial mission requirements. In addition, the system allows unbiased retrieval.